a varved sediment analysis of 1,000 years of climate...
TRANSCRIPT
A VARVED SEDIMENT ANALYSIS OF 1,000 YEARS OF CLIMATE CHANGE: LINNÉVATNET, SVALBARD
by
ALICE HELLER NELSON
Mea Cook, Advisor
A thesis submitted in partial fulfillment of the requirements for the
Degree of Bachelor of Arts with Honors in Geosciences
WILLIAMS COLLEGE
Williamstown, MA
MAY, 2010
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Acknowledgements
Writing a senior thesis has been an incredible experience, which has taught me
more than I ever would have expected. I would like to thank my thesis advisor Mea
Cook for guiding me through this process and for patiently answering all of my
questions. My research would not have been possible without funding from the Keck
Geology Consortium, the National Science Foundation, and Exxon-Mobile, thank you.
Thank you also to my summer field advisors, Al Werner, Steve Roof, and Mike Retelle
for taking me on an Arctic adventure and teaching me all about coring. I could not have
collected my samples on my own, and I am thankful to my entire Keck group for making
our trip to the Arctic so much fun and for sharing data and ideas throughout the year. A
special thanks to my coring partners Chris Coleman and Alex Nereson and to my polar-
barrack roommate Jacalyn Gorzcynski for being a great friend who helped keep morale
high on long, cold, and hungry days.
Thank you to the many people at Williams who have assisted me with this project
including my second reader Ronadh Cox for all of her helpful editing, Sharron Macklin
for helping me with all of my sediment images and Professor Klingenberg for teaching
me about statistics. I would also like to thank the entire Williams Geosciences
Department for introducing me to Geology and for making these past four years a lot of
fun.
For all of your support along the way, I would like to thank the Williams Ski
Team and the Williams Women’s Lacrosse Team, as well as my coaches Bud Fisher,
Aubrey Smith, Chris Mason, Alex Barrale, and Kate Hyde. I am also hugely thankful to
my friends and family for so much love and support.
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Abstract
In July 2009, we recovered a varved sediment core from 35 m in the deep main
basin of Linnévatnet, a high Arctic glacial lake in Svalbard. Arctic lakes are key
locations for studying climate records because the Arctic is highly sensitive to climate
change and because varves reflect seasonal and annual sedimentation rates. Previous
research in Linnévatnet has focused primarily on the proximal basin near the Linnéelva
(Linné River) inlet where it is difficult to distinguish annual sediment layers from event-
based layers. The lake core analysis will therefore contribute to our understanding of the
sediment stratigraphy in the deep main basin where varves reflect annual sedimentation.
Core IC09.1 is 39.8 cm long and contains 1154 ± 71 couplets, which we measured
in Photoshop using high-resolution (4800 dpi) scanned images of thin sections. The
varves range in thickness from 0.06 mm to 2.60 mm with a mean thickness of 0.34 mm.
To make a proxy climate record, we compared varve thickness to summer
temperature, summer precipitation, winter precipitation, and glacier mass balance from
the instrumental record. Summer temperature and summer precipitation show a
statistically significant positive correlation with varve thickness, though with a low
coefficient of determination (r2). We used thickness and a regression equation to estimate
climate pre-dating the instrumental record. If higher summer temperatures and increased
precipitation are related to thicker varves, then summer temperature and precipitation
have been greater in the 20th Century than in the past 1,000 years, and climate change in
the 20th Century has been greater than during the Little Ice Age and the Medieval Warm
Period.
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Table of Contents
Acknowledgements..................................................................................................................2
Abstract ........................................................................................................................................3
List of Figures.............................................................................................................................5
List of Tables ..............................................................................................................................6
Introduction ...............................................................................................................................7 Climate Change Worldwide and in the Arctic...........................................................................7 Setting .................................................................................................................................................. 12 Location...........................................................................................................................................................12 Climate.............................................................................................................................................................16
Sedimentary Processes.................................................................................................................. 18 Sediment Architecture ..............................................................................................................................18 Sediment Sources........................................................................................................................................20
Glacial and Climate History.......................................................................................................... 24 This Study........................................................................................................................................... 27
Methodology............................................................................................................................ 30 Field Methods.................................................................................................................................... 30 Coring...............................................................................................................................................................30 Dewatering ....................................................................................................................................................32 Transportation .............................................................................................................................................32
Laboratory Methods ....................................................................................................................... 34 Core Splitting ................................................................................................................................................34 Visual Stratigraphy and Core Selection..............................................................................................35 Sub‐sampling ................................................................................................................................................37 Thin Section Preparation .........................................................................................................................38 Varve Counting and Measuring .............................................................................................................40 Addressing Compaction ...........................................................................................................................43 Plutonium Dating ........................................................................................................................................43 Varve Thickness and Climate Correlations ......................................................................................44 Climate Reconstructions ..........................................................................................................................46
Results ....................................................................................................................................... 47 Age Model and Varve Thickness ...........................................................................................................47 Compaction....................................................................................................................................................50 Varve Thickness and Climate Correlations ......................................................................................51 Climate Reconstructions ..........................................................................................................................55
Discussion ................................................................................................................................ 58 Varve Thickness, Compaction, and Age Model ...............................................................................58 Varve Thickness and Climate Correlations ......................................................................................64 Climate Reconstructions ..........................................................................................................................69
Conclusion................................................................................................................................ 70
Works Cited ............................................................................................................................. 72
Appendix................................................................................................................................... 76
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List of Figures Figure 1: Surface temperature reconstruction................................................................... 11 Figure 2: Map of the ten-year average (2000-2009) temperature anomaly relative to the
1951-1980 mean........................................................................................................ 11 Figure 3: The Svalbard archipelago.................................................................................. 13 Figure 4: Spitsbergen is the archipelago’s largest island.................................................. 13 Figure 5: A 1936 aerial photo of Linnédalen courtesy of the Norsk-Polarinstitutt .......... 14 Figure 6: Bathymetric map of Linnévatnet....................................................................... 15 Figure 7: The Longyearbyen Airport temperature record for 1912-2009......................... 17 Figure 8: Weather statistics from the Linnedalen weather station (June, 2009 through
May, 2010)................................................................................................................ 17 Figure 9: Sediment trap data from winter 2004 to summer 2009 for the bottom trap at
mooring site C in the proximal basin........................................................................ 21 Figure 10: A bedrock map of Linnédalen from Perreault, 2009....................................... 22 Figure 11: Topographic map with 100 m contour intervals showing the location of
Linnévatnet. .............................................................................................................. 23 Figure 12: 1995 aerial photo of Linnébreen with terminus positions since 1936............. 26 Figure 13: Varve thickness for Pompeani’s cores G-08 B1 and G-08 B2 regressed against
July-August average temperature (Pompeani et al., 2009). ...................................... 29 Figure 14: Photos of the coring process............................................................................ 31 Figure 15: Cutting open the core tube using a rail-mounted router saw........................... 34 Figure 16: Core ICO9.1 on the left, and core ICO9.2 on the right. .................................. 36 Figure 17: Subsampling the core using a perforated metal tray. ...................................... 37 Figure 18: Section of a high-resolution scanned image of a thin section section............. 41 Figure 19: Example of a crack in the sediment slat. ......................................................... 42 Figure 20: Example of a thin section that was polished too thinly................................... 42 Figure 21: Example of a varve sequence where there is a lamination with ambiguous
grain size. .................................................................................................................. 43 Figure 22: Instrumental climatalogical and glacier mass balance records. ...................... 45 Figure 23: Varve thickness versus calendar year.............................................................. 48 Figure 24: Age model of the core showing calendar year versus depth. .......................... 48 Figure 25: Plutonium profile............................................................................................. 49 Figure 26: Bulk density data for a core from site G (Pratt, 2006). ................................... 50 Table 2: Summary of statistical correlations for varve thickness (x) regressed against
climatological parameters (y) and mass balance (y)................................................. 51 Figure 27: Correlations between varve thickness (x) and climatology (1912–2009) (y). 52 Figure 28: Correlations between smoothed thickness and climate................................... 54 Figure 29: Reconstructed summer (JJA) temperature is shown in blue. .......................... 56 Figure 30: Reconstructed summer (JJA) precipitation is shown in blue. ......................... 56 Figure 31: Summer (JJA) precipitation reconstructed from the correlation of smoothed
summer precipitation and smoothed varve thickness is shown in purple................. 57 Figure 32: Photoshop images of the two anomalous laminations..................................... 61 Figure 33: Graph showing the 137Cs profile for core a core from site G (Figure 6). ........ 63 Figure 34: Alkenone-inferred temperature from Kongressvatnet (Vaillencourt, 2010). .. 70
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List of Tables Table 1: Epson 1600 scanner settings............................................................................... 40 Table 2: Summary of statistical correlations for varve thickness (x) regressed against
climatological parameters (y) and mass balance (y)................................................. 51 Table 3: Summary of statistical correlations for the 11-year running mean of varve
thickness (x) regressed against the 11-year running mean of climatological parameters (y) and mass balance (y)......................................................................... 53
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Introduction
Varved sediment records have the potential to be used as proxies for climate
change because the lamination couplets reflect seasonal and annual sedimentation rates.
Proxy climate records are important because they enable us to determine climate histories
that predate instrumental monitoring. This research involves measuring varve
thicknesses from a sediment core taken from the deep main basin of Linnévatnet (Lake
Linné), a high Arctic glacial lake in Spitsbergen, Svalbard. Sediment layers are
compared to recent weather and glacier ablation records to determine the relationship
between varve thickness and climate. I use this correlation to extrapolate backward
through the sediment record and attempt to determine past climate patterns. The aim of
this work is to place current climate change within a historic context.
Climate Change Worldwide and in the Arctic
During the last 1,000 years, the earth has experienced three major climate events:
the Medieval Warm Period (MWP), the Little Ice Age (LIA), and ongoing 20th and 21st
century warming. The MWP is generally defined as a broad period of relatively warm
conditions centered around AD 1000 (National Research Council, 2006). Causes for the
MWP are not well understood (Bradley et al., 2003; Hunt, 2006), but multiple
reconstructions of surface temperature anomalies (Figure 1) show a period of warming
beginning in AD 900 and lasting through AD 1500 with the greatest extent of warming
occurring between AD 900 and AD 1200. Climate modeling by Hunt (2006) suggests that
temperature anomalies during the MWP are examples of naturally occurring climatic
variability. Possible forcing mechanisms include increased solar irradiance, changes in
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Arctic Oscillation circulation patterns, persistent circulation regimes (El Niña or El Niño)
and increased volcanism (Bradley et al., 2003). Climate reconstructions suggest that
during the MWP, northern Europe experienced warmer winters (Bradley et al., 2003) and
that drier conditions were felt globally (Olsen et al., 2010; Bradley et al., 2003).
The LIA is loosely defined as the time period between AD 1300 and 1850 (Figure
1) during which glacial advances occurred globally (Wanner et al., 2008), the earth
experienced the coldest temperatures of the last 12,000 years (Bradley et al., 2003), and
climate was generally wetter (Olsen et al., 2010). The strong cooling during the LIA was
most likely caused by a combination of factors including orbital, volcanic, and solar
forcing (Wanner et al., 2008) and decreased northern heat transport due to reduced Gulf
Stream flow (Lund et al., 2006).
Since the late 19th Century, the earth has been exhibiting a general warming trend
due to increases in solar irradiance and greenhouse gas concentrations (Mann et al.,
1998). During the mid-20th century, solar irradiance leveled off making greenhouse
forcing the dominant warming mechanism for the last 200 years, which characterizes the
20th century as a unique period of climate change (Mann et al., 1998). In spite of the fact
that orbital forcing trends toward general planetary cooling, the increase in anthropogenic
CO2 has caused global warming, that appears to be outside of the range of naturally
variability (Axford et al., 2009).
During the 20th century, global mean surface air temperatures have risen 0.6°C
with the largest temperature changes occurring in the Northern Hemisphere (National
Research Council, 2006; Serreze et al., 2000). From 1956 to 2005, the linear warming
trend has been 0.10–0.16°C per decade, almost twice the decadal warming trend from
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1906 to 2005 (IPCC Fourth Assessment Report, 2007). The Northern Hemisphere has
exhibited negative snow coverage anomalies since the 1980s and annual snow coverage
area has decreased 10% since 1972 (Serreze et al., 2000). Due to continually increasing
atmospheric CO2, combined with decreased snow and ice-albedo feedback mechanisms,
the earth will probably continue to warm and the greatest temperature anomalies are
predicted to occur in the Arctic (Kattsov et al., 2005).
Because of its sensitivity to climate change, the Arctic is a key location for
studying climate records. Albedo feedbacks, especially those related to the extent of
snow and sea-ice cover, are sensitive to warm temperatures and summer-insolation
anomalies (Kaufman et al., 2009); and these are the main cause of the short response time
in Arctic climate signals. The Arctic has been warming since the mid-19th century with
recent decades exhibiting an accelerated warming trend (Figure 2, Holmgren et al., 2009;
Serreze et al., 2000; Kaufman et al., 2009) coincident with the global rise in temperature
throughout the last 150 years (Wanner et al., 2008). In recent decades, the extent of
Arctic sea ice has decreased (Serreze et al., 2007; Comiso et al., 2008) and negative snow
cover anomalies have been recorded on both North America and Eurasia (Brown and
Mote, 2009).
Northern Hemisphere warming in the last decade has been anomalous within the
context of the last 1,700 years (Mann et al., 2008). In the last few decades, warming
trends in the Arctic have been approximately twice the global average (Hassol et al.,
2004) and the last ten years have been the warmest of the past 200 decades (Kaufman et
al., 2009). Greenhouse gases are interpreted to have been the dominant climate forcing
mechanism in the 20th century (Mann et al., 1998). The Arctic is therefore likely to
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continue warming into the future, and if warming continues at its present rate, the Arctic
Ocean could be ice-free in the summer within the next 30 years (Wang and Overland,
2009).
The Arctic serves as a climate gauge for the rest of the world, and studying past
climate in the Arctic enables us to test whether the warming that is occurring today is
truly anomalous on a millennial timescale. Understanding Arctic climate change will
help us to better predict future change for the rest of the globe.
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Figure 2: Map of the ten-year average (2000-2009) temperature anomaly relative to the 1951-1980 mean. The map shows that the Northern Hemisphere, and the Arctic in particular, have been experiencing anomalously warm temperatures (http://www.giss.nasa.gov/research/news/20100121/).
Figure 1: Surface temperature reconstruction. Smoothed reconstructions of large-scale (Northern Hemisphere mean or global mean) surface temperature variations from six different research teams shown along with the instrumental record. The black and blue curves are global temperature reconstructions and the red, yellow, green, and purple curves are Northern Hemisphere reconstructions. (National Research Council, 2006).
MWP LIA 20th
Century
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Setting
Location
During late July, 2009, a group of faculty and students of the Keck Geology
Consortium collected sediment cores from Linnévatnet on Spitsbergen in the Svalbard
archipelago (Figure 3). The land area of Svalbard is 61,020 km2, about sixty percent of
which is covered by ice (Norsk-Polarinstitutt). The main island of Svalbard, where
samples were collected, is Spitsbergen (Figure 4). The research area is Linnévatnet, in
Linnédalen (Linné Valley) on Spitsbergen’s western coast at the inlet of Isfjorden, the
island’s largest fjord (Figure 4).
The glacially eroded valley of Linnédalen runs north-south and is contained to the
east and to the west by mountain ridges, to the south by Linnébreen (Linné Glacier), and
to the north by raised marine beach terraces and Isfjorden (Figure 5). A small river,
Linnéelva, flows north from the terminus of the glacier to the lake’s inlet on its south end.
The lake outlet is to the north into Isfjorden and the Arctic Ocean.
Linnévatnet sits in a glacially eroded valley (Figure 5). It is a monomictic lake
that maintains a temperature below 4°C throughout most of the year (Bøyum and
Kjensmo, 1978). HOBO temperature loggers deployed at site C in 2004 (Figure 6)
recorded summer lake temperature in early June as 0.3°C, warming up to 5.5°C in the
beginning of August. By early September the lake temperature had dropped to just below
3.0°C and throughout the winter the lake maintained a temperature between 0.0 and
1.0°C (Steve Roof, personal communication). The lake is approximately 5 km long and 1
km wide with a surface area of 4.6 km2. The average lake depth is 18.6 m and the
maximum depth, in the north-central deep main basin, is 37 m (Bøyum and Kjensmo,
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1978). Our group recovered sediment cores from the main basin at a depth of
approximately 35 m (Figure 6).
Figure 3: The Svalbard archipelago. The archipelago is located within the box (Figure 4) between 74° and 81° N (Pompeani et al., 2009)
Figure 4: Spitsbergen is the archipelago’s largest island. The main settlement is Longyearbyen and the research area is Linnédalen at the inlet of Isfjorden (modified from Pompeani et al., 2009).
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N
Linnévatnet
LinnébreenGrønfjorden
Isfjorden Figure 5: A 1936 aerial photo of Linnédalen courtesy of the Norsk-Polarinstitutt
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Figure 6: Bathymetric map of Linnévatnet. The coring and mooring sites G, I, and H in the deep distal basin and coring and mooring sites F, E, D, and C in the proximal basin. The core analyzed in this study is from site I. Image courtesy of Steve Roof.
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Climate
The mean annual temperature on Svalbard is –4°C, but climate varies throughout
the archipelago. Primary weather statistics for Svalbard come from the airport in
Longyearbyen, which is the major settlement on Spitsbergen located to the east of
Linnédalen (Figure 4). Temperature measurements (Figure 7) have been made for
various locations on Spitsbergen (Barentsburg and Longyearbyen) for the last 100 years
and show an overall warming trend (Nordli and Kohler, 2004). In 2009, the average
temperature recorded in January at the Linnédalen weather station was –11°C and in July
was 7°C (Figure 8). Weather on Svalbard fluctuates rapidly due to the interaction
between warm water and air from the south and cold water and air from the northern
Polar Regions (Ingólfsson, 2006). The average precipitation on Svalbard is <190 mm,
characterizing the archipelago as an Arctic desert, but warm seawater from the Gulf
Stream and warm air currents from the south moderate climate on the western coast of
Spitsbergen such that it is generally warmer and more humid than elsewhere on the
archipelago.
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Figure 7: The Longyearbyen Airport temperature record for 1912-2009.
Figure 8: Weather statistics from the Linnedalen weather station (June, 2009 through May, 2010). Blue is precipitation (mm), green is solar radiation (W/m2), red is temperature (°C) and the blue box denotes the 2009 field season. Data courtesy of Al Werner.
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Sedimentary Processes
Sediment Architecture The lake sediments in Linnévatnet range from coarse silts to clays, most of which
enter the lake during the short melt period from mid July until early August during which
sedimentation rates are high and grain sizes are large (McKay, 2005). McKay (2005)
found that the largest peak in grain size (median grain size = 53 µm) is associated with
the spring melt and that these deposits are significantly coarser than sediments deposited
during the rest of the year (median grain size = 16 µm). Weather events strongly affect
the amount of sediment transport into Linnévatnet (Matell, 2006) as well as the grain size
in the proximal basin (Figure 6) where sedimentation rates are highest (1.5 mm/year) and
where there is a strong correlation between grain size and stream discharge (McKay,
2005). In the more distal basin (Figure 6), sedimentation rates are lowest (0.15 mm/year)
(McKay, 2005) and grain size is correspondingly lower and less affected by weather
events.
Like many glacial lakes, Linnévatnet has accumulated varved deposits throughout
most of the basin. Seasonal differences in grain size result in spring-winter couplets of
coarser and finer laminae, which can be counted as annual layers. When the spring melt
occurs in mid July, flow from Linnédalen into Linnévatnet is high and the grain size of
the sediment in transport is relatively large (McKay, 2005). Time-lapse cameras
maintained by the Svalbard REU program have shown that this melt event occurs
suddenly and rapidly causing the majority of snow in the valley to melt within a two-
week period. The lake ice breaks-up and Linnéelva carries snowmelt and precipitation
into Linnévatnet. Flow decreases from early August until mid September, as does
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sediment input. During the summer, flow in Linnéelva is driven by precipitation events,
high elevation snowmelt, and local melt from Linnébreen. Matell (2006) found that in
mid-late summer, glacial melt does not provide enough stream flow to transport
significant amounts of sediment so that high discharges in Linnéelva and sediment
transport are primarily controlled by episodic precipitation events (Matell, 2006).
In mid September, Linnéelva and Linnévatnet freeze-up, and lake inflow shuts
down. During the winter, when there is no wave motion and minimized currents, the
finest clay sediments settle out of suspension. In the deep basin, the seasonality of flow
produces a fining upwards couplet with sand and silt being deposited during the spring
and clay being deposited during the winter (Svendsen and Mangerud, 1997). The
difference in grain size between winter and spring creates a sharp contact, which enables
the couplets to be identified and counted as annual layers.
The varved sediment record in Linnévatnet has been described from core analysis
(Svendsen and Mangerud, 1997; Pompeani et al., 2009) and from sediment trap data
(Arnold, 2009; Gorczynski, 2010). The varves are well preserved because a lack of
biological activity prevents bioturbation from disturbing the sediments. While some
laminae may represent sediment gravity deposits recording discrete flow events, the
majority are annual varves, which can be distinguished from turbidites: and the number
of couplets correlates with the estimated age of the cores studied (Svendsen and
Mangerud, 1997).
Sediment traps, which use funnels to capture sediments from within the water
column, have been deployed year-round in Linnévatnet since 2004 (Figure 9). Traps
from site C (Figure 6), on the south end of the lake close to Linnéelva where grain sizes
20
are expected to be higher, reveal the seasonality of the sedimentation: the winter layer,
which is generally thinner than the summer layer, consists of fine-grained silt, 5–10 µm.
Spring sedimentation is medium to coarse silt, 15–45 µm, and follows a general fining
upward sequence (Arnold, 2009).
Sediment Sources The lake sediments in Linnévatnet, which come from the immediately adjacent
Linnédalen watershed, have a high mineral fraction and are mainly allocthonous and
inorganic (Bøyum and Kjensmo, 1980). Sources for sediment include direct erosion from
the bedrock surfaces as well as the reworking of glacial moraine features. Bedrock
sources (Figure 10) include coal-bearing Carboniferous sandstone (Billefjorden Group),
fossiliferous Carboniferous limestone (Nordenskiöldbreen Formation) and gypsum from
the Permian (Gipshuken Formation), and Precambrian metasediments from the Hecla
Hoek formation (Areno-argillaceous phyllite and St. Jonsfjorden sequence, Svendsen,
1997).
Most of the lake sediment is delivered by Linnéelva (Figure 11), which drains an
area of approximately 27 km2, including Linnébreen and several smaller glaciers (Snyder
et al., 2000). A second source of sediment is an alluvial fan to the east of the Linnéelva
inflow that builds directly into the lake. The fan drainage comes from snowmelt,
groundwater flow, and winter ice accumulation (Snyder et al., 2000). A third source of
sediment is a small, deglaciated cirque, and its ice-cored moraine, which are on the west
side of the lake (Snyder et al., 2000). Finally, small streams draining from the mountain
ridges to the east and to the west of the lake carry snowmelt from the mountain ridges
and transport a small, relatively insignificant amount of sediment (Snyder et al., 2000).
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Figure 9: Sediment trap data from winter 2004 to summer 2009 for the bottom trap at mooring site C in the proximal basin. Peaks in grain size correspond to the spring and summer months (Gorczynski, 2010).
22
Figure 10: A bedrock map of Linnédalen from Perreault, 2009.
23
Figure 11: Topographic map with 100 m contour intervals showing the location of Linnévatnet. Glaciated areas, including Linnébreen and several smaller cirques are indicated in gray. The sediment sources, labeled in red, are Linnéelva, the small cirque glaciers, an alluvial fan as well as several small mountain streams flowing off the ridges to the east and to the west of Linnévatnet (modified from Pompeani et al., 2009).
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Glacial and Climate History
Deglaciation of Svalbard began approximately 13,800 cal BP1 (calibrated years
before present) at the end of the late Weichselian glaciation (Forman et al., 1985). At this
time, Linnédalen was a tributary fjord to Isfjorden because relative sea level was
approximately 70 m higher than at present (Forman et al., 1985; Mangerud and Svendsen,
1990). Linnévatnet became emergent due to glacioisostatic rebound approximately 9,000
cal BP1 (Sandahl, 1986). Throughout the warm early and middle Holocene, Svalbard was
largely free of glaciers (Humlum et al., 2004). Precession during the Holocene resulted
in the Northern Hemisphere summer solstice no longer coinciding with the perihelion,
which caused high-latitude cooling and glacial advances (Wanner et al., 2008). Long-core
analysis from Linnévatnet (Svendsen and Mangerud, 1997) suggests that Linnédalen was
ice-free until approximately 3,000 cal BP1 when Linnébreen was formed and that
Linnébreen has existed continuously, though at different sizes, since that time (Svendsen
and Mangerud, 1997).
The most extensive glacial advances since the Holocene occurred on Svalbard
during the LIA (Snyder et al., 1999). In Linnédalen, glacial expansion occurred
throughout the 14th and 15th centuries with Linnébreen reaching its maximum extent
during the 19th century (Svendsen and Mangerud, 1997). Lichenometry suggests that
Linnébreen’s terminal moraine stabilized during two phases, 650 years ago and again
within the last few centuries (Werner, 1993). Historical accounts and oblique aerial
1 Recalibrated using Calib (http://intcal.qub.ac.uk/calib/calib.html) and Intcal 09 (Reimer et al., 2009).
25
photos suggest that Linnébreen was at, or close to, the Little Ice Age moraine until the
mid 1930s (Liestøl, 1969).
Aerial photo analysis shows that Linnébreen has retreated a total of 1,203 m since
1936, with retreat rates between 1961 and 2004 being at least double those between 1936
and 1961 (Figure 12; Schiff, 2004). Most glaciers worldwide are retreating (Dyurgerov
et al., 2009) and the retreat of Linnébreen is consistent with the records from other
glaciers on Svalbard, which have mass balances averaging –16 km3/year for the period
1961 to 1993 (Serreze et al., 2000).
26
Figure 12: 1995 aerial photo of Linnébreen with terminus positions since 1936. The terminal moraine is orange (Modified from Schiff, 2004).
27
This Study This research is part of an ongoing glacier-monitoring project in Linnédalen that
began in 2004 and will continue through the summer of 2012. The Svalbard Research
Experience for Undergraduates Program (REU) is directed by Alan Werner (Mount
Holyoke College) and Steven Roof (Hampshire College) and is funded by the National
Science Foundation in collaboration with the University Center on Svalbard. Fieldwork
in summer, 2009, was funded by the Keck Geology Consortium. Previous research has
included glacier ablation (Schiff, 2004), sediment transport (McKay, 2005; Matell 2006),
snow and ice melt, and sedimentation in Linnévatnet (Arnold, 2009). Research
conducted during the summer of 2009 was directed towards increasing the understanding
of sediment deposition in Linnévatnet through sediment trap studies (Gorczynski, 2010;
Coleman, 2010) and core analysis (Nereson, 2010), modeling glacier ablation (Dekker,
2010), evaluating alkenones as a record of past temperature in Kongressvatnet
(Vaillencourt, 2010), and determining lichen growth rates for the Linnébreen moraines
(Brown, 2010).
The majority of previous sedimentation research has focused on sediment traps
and sediment cores from the proximal basin, in the area near the Linnéelva inlet where
sedimentation rates are high. There are two major problems associated with cores from
the more proximal basin. First, the sediment, particularly at site C (Figure 6), is not very
conducive to coring. It is difficult to penetrate the sediment and recover a core without
disturbing the sediment stratigraphy because as the core tube is removed from the lake
bottom, some of the sediment slides back out of the bottom of the core tube. A core from
site C recovered by Arnold (2009) was missing the most recent years of sedimentation
28
and cores recovered from this site in the summer of 2009 were also without an intact
sediment-water interface.
Second, summer sedimentation in this proximal location is strongly affected by
precipitation-driven discharge events (McKay, 2005; Matell, 2006). In consequence, it is
difficult to distinguish the fining-upward signature of an event layer from the fining-up
pattern in true annual sedimentation couplets. Because of the potential for significant
confusion in interpretation of individual layers, it is difficult to use proximal cores as
climate-history proxies.
During the summer of 2008, therefore, two cores were collected from site G in the
deep main basin (Figure 6), where sedimentation rates are substantially lower because of
the distance away from the Linnéelva inlet. Individual precipitation-driven sediment
gravity flow event deposits are less likely to have persisted into the distal basin,
increasing the likelihood that laminae represent seasonal sedimentation regime changes.
Initial worries were that laminations in the deep-basin cores would be too diffuse for
analysis; but preliminary work suggests that, although the laminations are indeed thin
(mm to sub-mm), the stratigraphy is recognizably varved, and it is possible to count and
measure the annual layers (Pompeani et al., 2009). Varve thickness measurements were
found to correlate positively to summer (July-August) temperature from the instrumental
record, which dates to 1912 (Figure 13, Pompeani et al., 2009).
My thesis work represents continuation of the research into deep-basin cores,
building on the preliminary tests of Pompeani et al. (2009). This study analyzes the
lamination stratigraphy of a core from site I (Figure 6) and tests whether summer
temperature, summer precipitation, glacier ablation, and winter precipitation correlate
29
with varve thickness. The relationship between these parameters and sediment
stratigraphy is used to model past climate in Linnédalen from before the existence of the
instrumental record. The recent retreat of Linnébreen, placed within a context of changes
in climate over the last 1,000 years in Linnédalen, is used to further understand how the
Arctic responds to a warming climate.
Figure 13: Varve thickness for Pompeani’s cores G-08 B1 and G-08 B2 regressed against July-August average temperature (Pompeani et al., 2009).
30
Methodology
Field Methods
Coring
On July 29, 2009, we collected two sediment cores from site I at 35 m water depth
(Figure 6) using a Universal surface corer, deployed from the gunnels of a Zodiac (Figure
14). We used a percussion hammer to gently tap the core tube into the sediment, and
when it had penetrated approximately 30–60 cm, we carefully lifted the device back up.
We capped the bottom of the core tube before it broke the water surface to prevent
sediment loss. Both of the cores retrieved from site I retained a distinct sediment-water
interface, which indicates that the most recent layer of sediment was preserved. We
separated the core tubes from the coring device and capped the tops, then transported the
core tubes upright back to Isfjordradio by hand. Leaving the water in the tubes
throughout this process created a cushion, which prevented the surface of the sediment
from being disturbed.
31
Figure 14: Photos of the coring process. 1) Lowering the coring device into the water, 2) using the percussion hammer to tap the coring tube into the sediment, 3) capping the coring tube, and 4) recovering an intact sediment-water interface. Photos by Steve Roof.
32
Dewatering
The day after core retrieval, we siphoned the water out of the core tubes to
approximately 3 cm above the sediment-water interface. Although, care was taken to
minimize any jostling of the sediment surface, a small amount of sediment did become
suspended in the water. The following day, we made a horizontal cut with a soldering
iron to shorten the length of the core tube to approximately 3 cm above the water line. A
nail placed in the tip of the soldering iron and was used to melt through the plastic core
tubes, which cut down the core tubes without leaving any residue in the tube and without
disturbing the sediment in any way. We used a syringe to remove most of the remaining
water, and then carefully wicked up any additional water using the corner of an absorbent
paper towel. We left the cores to dry in a small, enclosed room with the heat turned up.
The cores dried for an additional four days and during this time the sediment surface
level lowered by about 2%.
Transportation
After 4 days of drying, we packed the core tubes for transport to Longyearbyen.
Plastic disks, cut from Ziploc bags, were placed on top of the sediment followed by a
layer (approximately 3-cm thick) of non-absorbent insulation material. We packed the
remaining space in the core tube (3–6 cm) with absorbent paper napkins. Care was taken
to completely pack the core tubes without depressing or disturbing the sediment to
minimize the amount of space in the tube so that the sediment would not shift during
transport. We capped both ends with core caps secured with electrical tape.
33
The core tubes traveled vertically in a plastic crate by boat from Isfjordradio to
Longyearbyen. Conditions were calm, so the tubes were not jostled. The following day,
we checked the core tubes and because the packing material was dry, we determined the
sediment to be stable. We recapped the core tubes, wrapped them in soft clothing, and
packed them horizontally in a footlocker for travel by air back to the United States. We
opened the core tubes in a lab at Mount Holyoke College and stored them in a cold room
(4°C). Some of the packing material in the core tubes was damp; but there was very little
sediment contamination on the insulation material, indicating that sediment did not shift
appreciably during transportation.
34
Laboratory Methods
Core Splitting I split the plastic core tubes length-wise using multiple passes of a rail-mounted
router saw (Figure 15). The saw cut deep enough to break the plastic but not penetrate
the sediment. After each side of the core tubes was cut, I split the sediment by passing
the core tubes through a taut piano wire, creating a clean cut which left each half of the
sediment core resting in the core tube.
Figure 15: Cutting open the core tube using multiple passes of a rail-mounted router saw. Photo by Alex Neresen.
35
Visual Stratigraphy and Core Selection
I photographed each sectioned core using a mounted Olympus Camedia C-8080
wide-zoom camera. I described their stratigraphies, taking notes on the depth and
thickness of notable lamina and describing their color and texture. The visual
stratigraphies of cores IC09.1 and IC09.2 matched each other well, with marker beds
appearing at the same depths in each (Figure 16). I chose core IC09.1 for further analysis
because it presented a longer record and because the domed sediment deformation was
more symmetrical than in core IC09.2 (Figure 16).
36
Figure 16: Core ICO9.1 on the left, and core ICO9.2 on the right. Marker beds in the two cores appear at the same depths, core IC09.1 is a longer sediment record with more uniform deformity, and was the focus of this study.
37
Sub-sampling I designated one half of the split core as the archive and put it away in cold
storage (4°C) for potential future use. I sub-sampled the other half for thin section
analysis, using perforated metal trays, which were created by hole-punching thin sheet
metal and folding the material into rectangular trays. The length of these trays varied
from 6 cm to 18 cm, but each was approximately 3 cm wide and 1 cm deep. I removed
the sub-samples by pressing the trays length-wise into the cut face of the sediment.
Because multiple trays were needed to subsample the length of the entire core, the trays
overlapped one another to ensure that all sediment layers were sampled (Figure 17). I
then removed the trays and sediment using a cheese-cutter-like device that passed a small
wire and metal strip underneath the trays. I sealed the trays with Saran Wrap, labeled
them according to their position along the core, placed them in a cooler, and transported
them to Williams College where they were stored at 4°C.
Figure 17: Subsampling the core using a perforated metal tray. The “cheese-cutter” device is on the table next to the right of the core. Photo by Steve Roof.
38
Thin Section Preparation I used a fluid-displacive resin-embedding technique to prepare the soft sediments
for sectioning. This technique, modified from Kemp et al. (2001), involved replacing the
water in the sediment with acetone and then embedding the samples with resin. This
method, while time intensive, is preferable to freeze-drying because the fine laminae are
continually supported, minimizing the potential for disturbance and cracking.
First, I split the sediment samples in half length-wise and transferred them from
their perforated metal trays to aluminum mesh boats (K&S Engineering, Item No.
15057). The smaller sample size was to ensure that the water would be completely
replaced by the acetone and resin, and the boats’ mesh provided greater opportunity for
fluid exchange.
I placed the sediment samples, inside their aluminum mesh boats, in high-density
polyethylene (HDPE) photo trays (8 3/4” x 6 7/8” x 1 1/2”, US Plastic Corp. Item No.
52050), resting on top of a layer of HDPE mesh (.32 mm x .32mm hole size, Industrial
Netting Part No. XV1347) to facilitate circulation of acetone and resin around the entire
samples (Lamoureaux, 1994). Next I placed the photo trays and Drierite desiccant inside
large, HDPE, lidded containers and stored them inside a fume hood. Over the course of
the next five days, I made a series of 15 acetone exchanges, at approximately 8:00 am,
1:00 pm, and 7:00 pm. I used enough acetone to entirely fill the photo trays and to cover
the samples completely and I used slightly more acetone at the 7:00 pm exchange to
compensate for the additional evaporation which would occur at night.
I made the exchanges by extracting the waste acetone with a large (60 ml),
polypropylene, catheter-tip syringe and transferred clean, lab-grade acetone (Reagent
39
ACS, USP/NF grade) into the photo tray with the same syringe. Throughout this process,
I avoided disturbing the sediment samples by slowly ejecting the acetone into the corner
of the photo tray. Some disturbance did occur as some sediment eroded from the mesh
boats and began to accumulate along the bottom of the photo tray. While this sediment
loss was minimal, it affected the laminae at the ends of each sample more than those in
the middle.
Following the final acetone exchange, I embedded the samples with resin through
a series of acetone-resin exchanges. The resin was composed of the following reagents,
vinyl cyclohexene dioxide (ERL 4206, 1.17 g/cm3), nonenyl succinic anhydride (NSA,
1.03 g/cm3), diglycidol ether of polypropyleneglycol (DER, 1.14 g/cm3), and
dimethylaminoethanol (DMAE, 0.88 g/cm3) in a recipe corrected from Kemp et al.
(2001) by Ellis (2006). I measured the reagents gravimetrically and mixed them together
each day immediately before adding them to the container. I diluted the initial resin
replacements with acetone to facilitate embedding and each additional acetone-resin
replacement contained a higher proportion of resin. I made the acetone-resin
replacements twenty-four hours apart over a period of five days and their proportions
were as follows: 50:50, 25:75, 10:90, with the final two replacements being entirely resin.
Like with the initial acetone exchanges, I removed and replaced the waste resin with a
polypropylene syringe and used enough resin to completely cover the samples.
Following the final resin replacement, I left the samples to sit in the resin for a week and
then cured them in a vented oven at 50°C for twenty-four hours.
40
After curing, the resin block was hard, translucent, and inert. I shipped the resin
block, containing the sediment samples, to Mount Holyoke College where a lab
technician cut down the samples and mounted them as large-format thin section slides.
Varve Counting and Measuring I scanned each slide onto a computer using an Epson Expression 1600 scanner
(Table 1). I opened the images in Photoshop and increased their brightness to make the
individual laminae more visible. I marked the varves with horizontal lines using the Pen
Tool in the Paths function. First, I rotated the image using the Ruler Tool so that the
varves were horizontal on the computer screen. Second, I created a vertical axis by
drawing a line perpendicular to the lamina. Third, I marked each varve by drawing a
horizontal line at winter-spring lamina boundary, which I identified by the abrupt change
in sediment color from a darker, finer grained layer to a lighter, coarser grained layer
(Figure 18). When this boundary was difficult to see on the computer screen, I consulted
a polarizing microscope because under crossed polars the spring layer has greater
birefringence then the winter layer. I calculated the thickness of each varve by measuring
the distance between each horizontal line segment with the Ruler Tool and then
converting the pixel length to millimeters. I calculated an error for my thickness
measurements by measuring a series of 10 varves 5 times each and averaging the
standard deviation of the measured thickness.
Table 1: Epson 1600 scanner settings
Document Type Reflective Document Source Document Table Auto Exposure Photo Image Type 24-bit color Quality Best Resolution 48000 dpi
41
Figure 18: Section of a high-resolution (4800 dpi) scanned image of a thin section section. Horizontal lines indicate the boundaries between varves and an example of a winter (darker and finer grained) layer is labeled in blue and a spring (lighter and coarser grained) layer is labeled in yellow.
I created an age model by counting the boundary lines drawn in Photoshop and
assigning a year to each varve. I took the most recent sediment layer at the top of the
core to be spring 2009 and worked backwards in time from that. Where individual varves
were difficult to distinguish, which sometimes happened due to cracking (Figure 19), due
to over-polishing of the thin section (Figure 20), or due to ambiguous differences in grain
size (Figure 21), I added 0.5 ± 0.5 years to the age model. This error accumulates
throughout the age model back in time such that the age of the older varves is less certain
winter
spring
1 mm
42
then the more recent varves. At 30 cm depth, there is 1.3 cm of sediment missing from
the record due to a piece of a thin-section being missing. For the interval of missing
sediment, I estimated the number of varves based on the mean varve thickness for rest of
that thin-section slide and calculated the uncertainty based on 75% of the variability in
varve thickness.
Figure 19: Example of a crack in the sediment slat. Cracking could have resulted in a varve not being counted or in a varve accidentally being added twice. To accommodate for this uncertainty, I added 0.5± 0.5 years to the age model.
Figure 20: Example of a thin section that was polished too thinly. The ends of the thin sections were often polished too thinly to be able to make out the laminations. This was generally not a problem because the sediment samples overlapped one another and I could use notable laminae to determine where the slides matched up.
1 mm
1 mm
43
Figure 21: Example of a varve sequence where there is a lamination with ambiguous grain size. In this sequence there are three examples of very clear varves. The winter layer is dark brown and is annotated with a blue line. The spring layer is lighter tan and is visibly coarser and is annotated with a blue line. In between the second and the third annotated varves there is an ambiguous layer that is gray, which I annotated with an orange line. In this instance I determined that the ambiguous gray layer was a varve with a thin poorly defined spring layer that is just barely visible in light tan. In instances such as this, I added 0.5± 0.5 years to the age model to account for my uncertainty.
Addressing Compaction
To estimate the extent of compaction that might have occurred in my core, I
compared the estimated mass accumulation rate (MAR) for the top 5 cm of my core to
the MAR for the bottom 31 cm of my core, which I calculated by multiplying bulk
density by mean varve thickness. I chose the initial depth of 5 cm because that is the
point at which bulk density changed appreciably. Ideally, I would have used bulk density
data from my own core, but since I did not conduct this laboratory procedure, I used bulk
density data from a 36 cm core taken from site G (Figure 6) in 2005 (Pratt 2006), which I
assumed to be similar to the bulk density of my core from site I.
Plutonium Dating Measurement of plutonium in sediments provides an independent age model by
pinning the year 1963, which was the peak of radionuclide fallout produced by
atmospheric nuclear weapons testing (Jaakkola et al., 2004). For Pu dating, I took
winter
spring
winter
spring
ambiguous
winter
spring
1 mm
44
continuous 0.5 cm thick samples from 0 to 7.5 cm that were about 0.5 g dry, which I
freeze dried and sent to Northern Arizona University where they were analyzed for the
1963 plutonium fall-out. The samples were dry-ashed at 600°C to remove any organic
matter and leached them with 2 mL of 16 M HNO3 with an added 242Pu yield tracer. The
leachates were diluted to 8 mL, filtered, and processed with TEVA resin to chemically
isolate 1.0 mL Pu fractions in aqueous ammonium oxalate solution. The analyses were
performed using a VG Axiom MC mass spectrometer in single-collector mode. A
“negative control” based on five samples of a Triassic sandstone was used to determine a
detection limit of 0.05 Bq/kg of 239+240Pu (Ketterer et al., 2004; Ketterer, personal
communication).
Varve Thickness and Climate Correlations
To make correlations between varve thickness and climate, I compared the varve
thickness measurements from 2009.0–1912.5 to known climatology data from the
instrumental record, which dates to 1912 (Figure 22). Because my ultimate goal was to
reconstruct past climate from varve thickness, I plotted the independent variable, varve
thickness, on the x-axis and the dependent variable, climatology, on the y-axis. From
these scatter plots, I used the Data Analysis function in Excel to calculate regression
statistics. I determined the correlations to be statistically significant if the observed
significance level (p-value) was less than 0.05 and for significant correlations, I plotted
the linear line of best fit. I also made correlations between smoothed thickness and
smoothed climate based on an 11-year running mean, which I calculated by averaging
five years of data on either side of each year’s thickness or climate value.
45
A B
C Figure 22: Instrumental climatalogical and glacier mass balance records. The instrumental temperature record (A) is from the Longyearbyen airport and dates from 2009–1912. The mean summer (JJA) temperature is shown in purple and the smoothed (11-year running mean) record is in orange. The instrumental precipitation (B) record is also from the Longyearbyen airport and dates from 2005–1912, the years 1944–1942 are missing from the record. The summed winter (Sep-May) precipitation and the smoothed record are shown in turquoise and green and the summer (JJA) precipitation and smoothed records are shown in blue and light blue. The Linnébreen glacier mass balance data (C) dates from 2005–1971 and is shown in green along with the smoothed record in purple.
46
Climate Reconstructions
For climate reconstructions, I used the equation of the linear line of best fit for the
statistically significant correlations between varve thickness and climate. The equations,
in the format y=mx+ b, calculate the reconstructed climate (y), by multiplying the slope
of the line of best fit (m) with varve thickness (x) and adding the y-intercept (b). I
calculated a confidence interval for the climate reconstructions using the equation:
±1.96 ˆ σ 2 1n
+x − x( )2
x1 − x( )2∑
⎛
⎝
⎜ ⎜
⎞
⎠
⎟ ⎟
where ˆ σ 2 = the square of the residual standard error, n = the sample size, x= the varve
thickness measurement, and x = the mean varve thickness.
47
Results
Age Model and Varve Thickness
Sediment core IC09.1 is 39.8 cm long and 1.3 cm of sediment are missing from
the thin sections at a depth of approximately 30 cm due to thin section processing. The
core contains a total of 1154 ± 71 varve couplets. The measured varves range in
thickness from 0.06 mm to 2.60 mm with a mean thickness of 0.34 mm and a standard
deviation of 0.21 mm (Figure 23). The error, based on reproducibility, associated with
varve thickness is 0.005 mm.
The age model of the measured varves is shown in Figure 24 and the oldest layer
measured dates to AD 797.5 ± 71.0 years. The age model places the year 1963 at a depth
of 3.0 cm, which is consistent with plutonium dating, which indicates that 1963 occurred
between 3.0 and 3.5 cm depth (Figure 25).
The mean varve thickness for the 20th Century is 0.50 mm with a standard
deviation of 0.32 mm and a standard error of 0.03 mm and is thicker than the mean
thickness for the rest of the core. The mean varve thickness for the LIA (AD 1850–1300)
is 0.31 mm with a standard deviation of 0.16 mm and a standard error of 0.01 mm, which
is about the same as for the MWP (AD 1200–900) where the mean thickness is 0.30 mm
with a standard deviation of 0.24 mm and a standard error of 0.02 mm.
48
Figure 23: Varve thickness versus calendar year. The thinner blue line is the measured varve thickness and the thicker red line is varve thickness smoothed with an 11-year running mean. The anomalously thick layers at AD 1249 and AD 1056.5 are believed to be event beds rather than varves.
Figure 24: Age model of the core showing calendar year versus depth. The blue lines represent the uncertainty showing the maximum and minimum age at each depth. The dotted lines represent a gap in the sediment record due to a missing piece of thin section, the change in slope is due to the greater uncertainty associated with the missing section. Labeled in red is the 20th Century, in blue the Little Ice Age (AD 1300-1850), and in green the Medieval Warm Period (AD 900-
49
1200).
Figure 25: Plutonium profile. The core intervals between 4.5-5.0 and 7.0-7.5 cm contain no detectable 293+240Pu. Plutonium is first detected in the 4.0-4.5 cm interval (0.06 ± 0.01 Bq/kg 239+240Pu), reaches a maximum in the 3.0-3.5 cm interval (13.80 ± 0.09 Bq/kg 239+240Pu), and is detectable at decreasing levels in all layers up to the surface. Based upon this information, it is evident that the 1963 peak is present in the 3.0-3.5 cm horizon. Plutonium dating courtesy of Michael Ketterer at Northern Arizona University.
50
Compaction The average bulk density for the top 5 cm of a core from site G (Pratt, 2006) is
0.87 g/cm3 and for the bottom 31 cm is 1.04 g/cm3 (Figure 26). When bulk density is
multiplied by mean varve thickness for the top 5 cm of my core (mean thickness = 0.052
cm) and the subsequent 31 cm of my core (mean thickness = 0.032 cm), the MAR for the
top is 0.045 g/cm2, which is 27% higher than 0.033 g/cm2, the MAR for the bottom.
Figure 26: Bulk density data for a core from site G (Pratt, 2006). From left: dry bulk density (g/cm3), percent organic content, percent carbonate content, and magnetic susceptibility (si).
51
Varve Thickness and Climate Correlations
The varve-thickness measurements are correlated with climatology data from the
Longyearbyen airport and to mass balance data from Linnébreen (Table 2). The positive
correlations between varve thickness and summer temperature (Figure 27, A), and
between varve thickness and summer precipitation (Figure 27, B) are statistically
significant, however each correlation is associated with very low r2 values. The
correlation between varve thickness and mass balance (Figure 27, C) is statistically
significant but not meaningful because the r2 value is so low and the correlation between
varve thickness and winter (Sep-May, defined by monthly temperatures below freezing)
precipitation (Figure 27, D) is not statistically significant.
Table 2: Summary of statistical correlations for varve thickness (x) regressed against climatological parameters (y) and mass balance (y).
r r2 p m b
Summer Temperature (JJA) 0.181 0.033 0.058 0.398 4.214
Summer Precipitation (JJA) 0.217 0.047 0.028 17.989 36.022
Winter Precipitation (Sep-May) 0.103 0.011 0.295 14.666 121.031
Linnébreen Mass Balance 0.101 0.010 0.0001 0.110 -0.510
52
A B
C D
Figure 27: Correlations between varve thickness (x) and climatology (1912–2009) (y). Varve thickness has a statistically significant positive correlation to average summer (JJA) temperature (A), and to summer (JJA) precipitation (B). Varve thickness does not correlate meaningfully to mass balance (C) or significantly to winter (Sep-May) precipitation (D).
53
The 11-year running mean of the varve thickness measurements is also correlated
with the 11-year running mean of the climatological parameters. The correlation between
the running mean of varve thickness and the running mean of summer (JJA) precipitation
is statistically significant with an r2-value of 0.28 (Figure 28, A). The correlations
between the running mean of varve thickness and the running mean of summer (JJA)
temperature (Figure 28, B), winter precipitation (Figure 28, C), and mass balance (Figure
28, D) are not statistically significant.
Table 3: Summary of statistical correlations for the 11-year running mean of varve thickness (x) regressed against the 11-year running mean of climatological parameters (y) and mass balance (y).
r r2 p m b
Summer Temperature (JJA) 0.126 0.016 0.205 0.319 4.244
Summer Precipitation (JJA) 0.529 0.280 6.84x10-8 40.835 24.931
Winter Precipitation (Sep-May) 0.171 0.029 0.105 18.003 118.828
Linnébreen Mass Balance 0.120 0.014 0.527 -0.050 -0.370
A B
C D Figure 28: Correlations between smoothed (11-year running mean) thickness and climate. The 11-year running mean of varve thickness has a statistically significant positive correlation with the 11-year running mean of summer (JJA) precipitation (A). Smoothed thickness against summer (JJA) temperature (B), mass balance (C), and winter (Sep-May) precipitation (D) does not correlate significantly.
55
Climate Reconstructions The statistically significant correlations between annually resolved varve
thickness and summer (JJA) temperature (Figure 27, A) and precipitation (Figure 27, B)
can be used to make climate reconstructions of summer (JJA) temperature (Figure 29)
and precipitation (Figure 30) from before the instrumental record. The mean
reconstructed summer (JJA) temperature is 4.34°C. For the MWP and the LIA it is
4.33°C and for the 20th Century it is 4.41°C. The mean reconstructed summer (JJA)
precipitation is 42.04 mm, for the MWP it is 41.28 mm, for the LIA it is 41.55 mm, and
for the 20th Century it is 45.09 mm. The instrumental summer (JJA) temperature and
precipitation data fall within the confidence interval for the reconstructed records. A
reconstruction of summer (JJA) precipitation can also be made from the statistically
significant correlation between the smoothed (11-year running mean) varve thickness and
the smoothed summer (JJA) precipitation (Figure 31).
56
Figure 29: Reconstructed summer (JJA) temperature is shown in blue. The green represents the confidence interval for the reconstructed temperature, and the red is the instrumental record.
Figure 30: Reconstructed summer (JJA) precipitation is shown in blue. The confidence interval for the reconstructed precipitation is green, and the instrumental record is red.
57
Figure 31: Summer (JJA) precipitation reconstructed from the correlation of smoothed summer precipitation and smoothed varve thickness is shown in purple. The 11-year running mean of the reconstruction is shown in orange, the instrumental precipitation record is shown in red, and the uncertainty for the reconstruction is shown in blue.
58
Discussion
Varve Thickness, Compaction, and Age Model
The varve thickness measurements show an increasing trend through time with
the highest mean thicknesses being found in the 20th Century (Figure 23). In thinking
about this trend towards thicker varves at the top of the core, we need to address the issue
of compaction. We would expect the varves at the top of the core (corresponding to the
20th Century) to be thicker than the varves at the bottom of the core because the top has
experienced less post-depositional sediment compaction. Because the MAR for the top of
the core (0.045 g/cm2) is 27% greater than the MAR for the bottom of the core (0.033
g/cm2), we are confident that the trend towards thicker varves in the 20th century can be
in part attributed to environmental factors aside from compaction such as changes in
climate.
If compaction were the sole factor contributing to changes in varve thickness,
then we would expect to see a hockey stick shaped varve thickness graph. Instead, we
see changes in varve thickness throughout the sedimentary record including a trend
towards increasing varve thickness at the end of the MWP, a gradual trend towards
decreasing thickness throughout the beginning of the LIA, and a trend towards increasing
thickness beginning in AD 1850 and accelerating through the 20th century (Figure 23).
These observed trends are expected because varve thickness is a function of the
sedimentation rate in Linnévatnent, which is controlled by climate. The primary source
of sediment to Linnévatnet is Linnéelva, and the amount of sediment carried by
Linnéelva is a function of discharge. During periods of warming, we would expect to see
59
higher discharges in Linnéelva due to warmer temperatures causing greater glacier
ablation and snowmelt. During periods of cooling, we would expect to see lower varve
thicknesses because decreased ablation and snowmelt cause lower discharges and
decreased sedimentation.
The 20th Century has a higher mean varve thickness (0.50 mm) than the LIA (0.31
mm), and the LIA has a lower mean varve thickness than the rest of the core (0.34 mm).
From temperature reconstructions and moraine evidence, we know that the LIA was one
of the coldest time periods in the last 12,000 years (Bradley et al., 2003) during which
there were global glacier advances (Wanner et al., 2008) including the advance of
Linnébreen on Svalbard (Snyder et al., 1999). In Linnédalen, during a time of cold
temperatures and glacial advance, we would expect lower varve thicknesses because
longer winters, shorter springs, positive mass balance, and less snowmelt would cause
decreased discharge in Linnéelva and lower sediment fluxes in Linnévatnet. It is also
possible that periods of glacial advance could be associated with increased sedimentation
because an advancing glacier erodes bedrock and thus might cause higher suspended
sediment loads during the basal melt season (David Dethier, personal communication).
Because the MWP was warmer, we would expect it to have a higher mean varve
thickness than the LIA, but it did not. The MWP is associated with warmer winters in
northern Europe (Bradley et al., 2003) and drier conditions globally (Olsen et al., 2008).
Warmer temperatures in Linnédalen would cause increased glacier and snowmelt,
contributing to higher discharges in Linnéelva and greater sedimentation in Linnévatnet.
One possible explanation for the low varve thicknesses during the MWP (0.30 mm) could
be that while winters might have been warmer in some places, they might not have been
60
warm enough to decrease the duration of winter at the high latitudes. A second
explanation is that the drier conditions caused decreased discharge (due to lower
precipitation rates), which offset the influence of warmer temperatures causing increased
discharge (due to increased snowmelt). A third explanation is that the calculated mean
varve thickness for the MWP is not reflexive of the observed trend, which shows
thickening varves during the end of the time period, because the sediment record during
the MWP is incomplete (Figure 23).
The varve thickness record shows two anomalously large measurements at AD
1249 and AD 1056.5 (Figure 23). One explanation for these anomalies is that I
misinterpreted some of the varves and measured multiple varves as one. Another
explanation is that the thickness of the anomalous laminae is not a function of climate.
There are several fan deltas, which prograde into Linnévatnet and it is possible that the
very thick varves are the result of a subaqueous slope failure causing a thick sediment
layer, which is an event and not a varve.
The lamination anomaly at AD 1249 does not match the varved sediment pattern
that surrounds it, and it also does not look like multiple varves that were miscounted as
one (Figure 32, A). In this section of the sediment record, there is a distinct varve pattern
where the coarser spring layers are light gray and the finer winter layers are dark gray.
This pattern is interrupted by a much thicker tan layer, which shows a generally fining-up
pattern typical of a turbidite. Because this anomalous lamination looks distinctly
different from the varves that surround it, I am confident that it is not a varve, and I
therefore excluded it from my climate reconstructions.
61
The anomaly at AD 1056.5 is similar to the one from AD 1249 in that it doesn’t
fit in with the surrounding sediment pattern, and it also does not look like multiple
varves, which were misattributed as one (Figure 32, B). The surrounding sediment
pattern is alternating light and dark brown bands corresponding to summer and winter
layers, but the anomaly is much thicker and is more of an orange-tan color. Like the
anomaly at AD 1249, this lamination shows a generally fining-up sequence typical of a
turbidite and so it was also omitted from the climate reconstructions.
Another commonality between these two anomalies is that they are cracked. The
cracked space was not included in the thickness measurement, but it is possible that the
process of cracking stretched out the sediment to make it thicker than it would have been
otherwise. It is also possible that the cracking is related to the anomaly because a coarser
turbidite layer would have less cohesion than the surrounding varves and would therefore
be more likely to crack during thin section preparation.
A B
Figure 32: Photoshop images of the two anomalous laminations. The anomaly at AD 1249 (A) is 2.60 mm thick and the anomaly at AD 1056.5 (B) is 1.74 mm thick. Both anomalous laminations are probably turbidites rather than varves.
1 mm 1 mm
62
The varve thickness measurements from site I (Figure 23) have a mean thickness
of 0.34 mm with a standard deviation of 0.21 mm, and these measurements are
inconsistent with Pompeani et al.’s (2009) from site G (Figure 6) who found a mean
varve thickness of 1.4 mm with a standard deviation of 0.6 mm. Pompeani’s varve
thicknesses are three times thicker than my own and it is difficult to figure out why our
measurements differ by so much. I had thought that perhaps Pompeani had made a
mistake when converting between pixel length and millimeters, but his varve thicknesses
add up to the length of his core, so it is unclear where the error occurred.
I am confident in my own interpretation and measurement of varves because my
results are consistent with Plutonium dating (Figure 25) which indicates that 1963
occurred from the sediment sample at 3.0–3.5 cm depth, and my age model placed 1963
at 3.0 cm depth. Additionally, my results are supported by Cesium-137 dating by
Nereson (2010) for a core taken at site G (Figure 6) also during the summer of 2009,
which found a 137Cs maximum at 2.90 cm corresponding to the year 1963–64 (Figure 33).
Nereson (2010) found the 137Cs spike at a slightly shallower depth than my Pu spike,
which is consistent with the expected lower sedimentation rate at site G than at site I
(Figure 6) due to distance away from the Linnéelva inlet.
63
Figure 33: Graph showing the 137Cs profile for core a core from site G (Figure 6). The profile indicates that the year 1963 occurred at 2.9 cm depth which is consistent with my Pu dating at site I, which indicated that the year 1963 occurred at 3.0 cm depth (Nereson, 2010).
64
Varve Thickness and Climate Correlations I expected to see a positive correlation between varve thickness and each of the
climatological parameters that I tested, average summer (JJA) temperature, summer
precipitation, and winter (Sep-May) precipitation, because each relates to discharge.
Increased summer temperature influences discharge by causing greater glacier and
snowmelt. Greater summer precipitation influences discharge directly by raising river
levels and indirectly by accelerating melt. Winter precipitation influences discharge
because the amount of accumulated snow determines the amount of melt in the spring,
which then contributes to flow in Linnéelva. I expected to find a negative correlation
between varve thickness and glacier mass balance because a more negative mass balance
indicates a greater amount of melt which would correspond to higher discharge.
The correlations between varve thickness and summer (JJA) temperature and
between thickness and summer (JJA) precipitation were positive and statistically
significant, but with very low r2-values (Figure 27, A and B). The correlations between
varve thickness and mass balance and between thickness and winter (Sep-May)
precipitation were not statistically significant (Figure 27, C and D).
As expected, varve thickness correlates positively with summer (JJA) temperature
because increased temperatures cause greater glacier ablation and increased snowmelt,
both of which contribute to higher discharges and greater sedimentation fluxes (Figure
27, A). The relationship between thickness and summer (JJA) temperature can only
explain 3% of the variability in the varve thickness measurements, so other factors have
dominant control of thickness. One possible explanation for this could be that the
intensity of the spring melt is more influential than average summer temperature. A
65
possible way to test for this could be to compare varve thickness to June temperature or
to summer positive degree-days. When I correlated June temperature with thickness, I
found that while the relationship is statistically significant (p=3.19x10-21), it explains less
than 3% of the variability (r2=0.027).
Varve thickness correlates positively with summer (JJA) precipitation with the
highest r2-value of all of the annually resolved correlations (Figure 27, B). Summer (JJA)
precipitation directly influences discharge and Matell (2006) found that in mid-late
summer, discharge is primarily a function of precipitation. While the r2-value for this
correlation was higher than the others, the relationship between varve thickness and
summer (JJA) precipitation only explains 5% of the variability in thickness, indicating
that precipitation is not the dominant control on varve thickness. A possible explanation
for this is that, the intensity of the precipitation is more influential than the overall
amount of precipitation added up over three months (JJA). For example, a summer with
lower precipitation that is stormier, in which precipitation is concentrated into a couple of
storm events might cause greater sediment input than a summer in which precipitation is
higher, but evenly distributed so that the discharge is constant. While I have not analyzed
precipitation intensity, I do know that Linnédalen received higher than average rainfall
during the summer of 2004 (70 mm), but varve thickness for the same year (0.42 mm)
was below the 20th century average. It could be that the summer of 2004, despite the high
amount of rainfall, was not as stormy as some other summers.
I expected varve thickness to correlate negatively to glacier mass balance because
more negative mass balance values, indicating glacier ablation, would cause increased
discharge corresponding to thicker varves (Figure 27, C). The lack of correlation is
66
probably because Linnébreen is relatively small compared to the 27 km2 Linnéelva
watershed and would therefore have a comparatively small influence on discharge and so
changes in Linnébreen mass balance are not likely to show up in the very finely
laminated sediment record.
I expected varve thickness and winter (Sep-May) precipitation to have a positive
correlation because greater winter snow accumulation would lead to a greater quantity of
snowmelt and thus higher discharges (Figure 27, D). The reason why the correlation
between thickness and winter precipitation was not statistically significant might be that
the intensity of the spring melt is not related to total snow accumulation.
In addition to correlating annual climatology with annually resolved varve
thickness, I also made correlations between an 11-year running mean of the climate
parameters and an 11-year running mean of the varve thickness measurements. I made
these smoothed correlations in case I was somehow off by one or more years in my age
model, which would have completely thrown off my annual correlations because there is
so much year-to-year variability in the climatology (Figure 22), and also to see if any of
the climate parameters had a greater influence on varve thickness when considered over a
longer time period.
The only 11-year running mean correlation that is statistically significant is the
correlation between varve thickness and summer precipitation (Figure 28, A). When this
correlation is smoothed, the r2-value increases to 0.28 and the p-value decreases to
6.835x10-8 indicating that the correlation is significant, and that smoothed summer
precipitation explains almost 30% of the variability in the smoothed thickness record.
The reason for the greater correlation when the records are smoothed is probably not due
67
to compensating for the age model being off by a year because the correlations do not
improve for any of the other parameters. The improvement in correlation is probably due
to the influence of precipitation over a greater time span, which suggests that
precipitation is stored within the watershed over a longer period than one year. An
example of this theory is seen in the sediment record for 2004 and 2005. The summer of
2004 had higher than average precipitation (70 mm), but lower than average varve
thickness (0.42 mm). Interestingly, the following summer had lower precipitation (40
mm), but higher than average varve thickness (0.70), which supports the theory that there
may be a time lag between precipitation and its influence on varve thickness.
What is interesting about this correlation is that the thickness measurements,
which fall roughly in the middle of the observed spectrum, between 0.40 and 0.50 mm,
are associated with a large range in precipitation values, from >25 mm to <60 mm. On
the other hand, the thickness measurements that fall on the extreme ends of the observed
spectrum, >0.35 mm and <0.60 mm, are all associated with very low variability in
precipitation such that almost all of the thinner varves are associated with relatively dry
summers (>35 mm) and almost all of the thicker varves are associated with wetter
summers (<50 mm). This observation suggests that summer precipitation is most
influential when varve thicknesses are either very thin or very thick, but for varves with
an average thickness, there is a great range in possible precipitation levels and therefore
there must be other controlling factors.
The other smoothed correlations did not show statistical significance. The
explanation for the lack of correlation between smoothed winter precipitation and
smoothed thickness and between smoothed glacier mass balance and smoothed thickness
68
is probably similar to the explanation stated above for the lack of annual correlation
between the same parameters. It is interesting that the correlation of summer temperature
and varve thickness is statistically significant at an annual resolution, but not at a
smoothed 11-year resolution. This lack of correlation suggests that summer temperature
for a given year is not influenced by summer temperature of past or future years, which
may be because the majority of the snow melts in the valley by the end of the summer
regardless of differences in winter snow accumulation or summer temperature and so
there is no hold-over influence from previous years.
The comparisons between varve thickness and climatological parameters
including mass balance, indicate that while some correlations are statistically significant,
at an annual resolution, the parameters which I have addressed each explain less than 5%
of the variability in thickness, and combined they account for less than 10% of the
variability. When the records are smoothed with an 11-year running mean, summer (JJA)
precipitation can explain 28% of the variability in varve thickness, but there must be
additional dominant factors influencing thickness.
These results are consistent with sediment trap data from 2004–2009 (Figure 9),
which show year-to-year variability in varve thickness that is not yet well understood.
Arnold (2009) analyzed four years of sediment trap data and found that looking at
weather trends (temperature, precipitation, and solar radiation) alone over the four years
did not provide conclusive evidence for the driving force of sedimentation. The
relationship between climate and sedimentation cannot explain as much of the variability
in varve thickness measurements as we had expected, but the long-term trends in varve
thickness are significant and do show that the varves in the 20th century are thicker than
69
those in the rest of the core. Even though we do not fully understand the driving
mechanisms for varve thickness, we can conclude that the 20th century is a unique period
of change that is different from the LIA and MWP.
Climate Reconstructions
The climate reconstruction based on the correlation with the highest r2-value
(0.28) is the 11-year smoothed reconstruction of summer precipitation (Figure 30).
While there is uncertainty associated with this reconstruction, the correlation indicates
that very thin and very thick varves can be well explained by changes in summer
precipitation (Figure 28, A). The reconstruction suggests that precipitation has varied
through time with a greater number of wet summers occurring in the 20th century than in
the past 1,000 years.
The two annually resolved climate reconstructions are created using correlations
with low r2-values, which means that the reconstructions are not robust. In addition to
the uncertainty, the reconstructed records do not show the year-to-year magnitude in
variability seen in the instrumental record. The reason that the variability is lost is
because at each temperature level or amount of precipitation, there is a range in varve
thicknesses. Even with these two caveats, the reconstructions show that the 20th century
has had the warmest and wettest summers (JJA) of the past 1,000 years and the
magnitude of climate change which is occurring today is greater than the change which
occurred during the LIA and the MWP. The annual temperature reconstruction is also
well supported by a climate reconstruction by Vaillencourt (2010) showing alkenone-
inferred temperature from Kongessvatnet (Figure 34), which is approximately 3 km to the
southeast of Linnévatnet.
70
Figure 34: Alkenone-inferred temperature from Kongressvatnet (Vaillencourt, 2010).
The reconstructions can only provide an estimate of what the summer climate in
Linnédalen might have been like before the instrumental record. Each reconstruction is
created from a correlation with a low r2-value, which means that the variability in varve
thickness cannot be fully explained by the tested climatology parameters. Because the
variability in varve thickness through time can only be partly attributed to changes in
summer temperature and precipitation, the reconstructions can only tell a partial story of
past climate. Even though the story is incomplete, what the sediment record tells us is
still valuable and interesting. While a mathematical equation cannot fully explain trends
in varve thickness, we do see a pattern towards thicker varves in the 20th century, which
cannot be entirely explained by compaction and that is unique to the last 1,000 years.
71
Conclusion
Sediments in the deep main basin of Linnévatnet are varved and plutonium dating
confirms that each couplet represents one year of sedimentation. Varve thickness has a
statistically significant positive correlation to summer (JJA) temperature and
precipitation, but low r2-values indicate that additional factors explain over 90% of the
variability in varve thickness. Varve thicknesses vary greatly year-to-year and the
relationship between climatology and thickness is not well understood. The low r2-values
create a large uncertainty in the climate reconstructions and the reconstructions mute the
yearly variability in climate. Even with the limitations of the reconstructions, trends in
varve thickness suggest that summer (JJA) temperature and precipitation have been
greater in the 20th Century than in the past 1,000 years and that climate change in the 20th
Century has been greater than during the Little Ice Age and the Medieval Warm Period.
Because the Arctic is highly sensitive to climate change, it is often used as a gauge for the
rest of the world, and this research suggests that the climate change we are experiencing
now is of a greater magnitude than during periods of change in the recent past.
72
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Appendix Age model, thickness, instrumental climate, and climate reconstructions Error is cumulative, JJA = June, July, August, Winter = September-May, Recon = Reconstructed, RM = 11 year running mean
Year
Error (±)
Thickness (pixels)
Thickness (mm)
Depth (mm)
JJA Temp (°C)
JJA Precip (mm)
Mass Balance (m/year)
Winter Precip (mm)
Recon Temp (°C)
Recon Precip (mm)
RM Recon Precip (mm)
2009.
0 0.0 24 0.13 0.13 5.00 4.26 38.31 20
08.0 0.0 96 0.51 0.63 4.30 4.41 45.16
2007.
0 0.0 272 1.44 2.07 5.70 4.77 61.91 20
06.0 0.0 452 2.39 4.47 5.70 5.14 79.02
2005.
0 0.0 132 0.70 5.16 5.97 40.4 -0.89 82.90 4.49 48.59 51.02 20
04.0 0.0 80 0.42 5.59 5.43 69.9 -1.05 133.00 4.38 43.64 51.74
2003.
0 0.0 92 0.49 6.07 5.40 26.4 -0.85 167.90 4.40 44.78 51.40 20
02.0 0.0 196 1.04 7.11 6.10 40.6 -0.55 144.70 4.62 54.68 49.23
2001.
0 0.0 184 0.97 8.09 5.43 40.6 -0.40 153.00 4.59 53.54 45.73 20
00.0 0.0 48 0.25 8.34 4.47 43.5 -0.03 150.10 4.31 40.59 45.24
1999.
0 0.0 100 0.53 8.87 4.67 61.4 -0.31 78.60 4.42 45.54 45.16 19
98.0 0.0 60 0.32 9.19 5.97 14.4 -0.86 112.30 4.34 41.73 44.89
1997.
0 0.0 44 0.23 9.42 4.20 67.6 -0.52 135.40 4.30 40.21 43.77 19
96.0 0.0 84 0.44 9.86 4.27 58.4 -0.08 189.90 4.39 44.02 43.22
1995.
0 0.0 80 0.42 10.29 5.03 27.4 -0.79 94.30 4.38 43.64 43.27 19
94.0 0.0 72 0.38 10.67 3.93 89.4 -0.15 153.60 4.36 42.88 42.98
1993.
0 0.0 64 0.34 11.01 5.57 34.5 -0.96 191.90 4.35 42.11 43.07 19
92.0 0.0 78 0.41 11.42 4.60 65.7 -0.17 121.90 4.37 43.45 43.81
1991.
0 0.0 126 0.67 12.09 4.80 59.8 0.12 196.20 4.47 48.02 43.55 19
90.0 0.0 53 0.28 12.37 4.97 26 -0.59 134.90 4.32 41.07 43.72
1989.
0 0.0 70 0.37 12.74 4.17 65 -0.35 100.30 4.36 42.69 45.32 19
87.0 0.0 69 0.37 13.10 5.07 49.9 -0.51 135.00 4.36 42.59 45.87
1986.
0 0.0 122 0.65 13.75 3.67 47.1 0.23 80.60 4.47 47.64 45.72
77
1985.
5 0.5 57 0.30 14.05 5.13 43.1 -0.27 179.30 4.33 41.45 45.68 19
84.5 0.5 98 0.52 14.57 5.07 27.2 -0.52 165.80 4.42 45.35 47.00
1983.
5 0.5 240 1.27 15.84 4.80 40.1 -0.71 125.00 4.71 58.87 47.92 19
83.0 1.0 122 0.65 16.48 4.80 40.1 -0.22 125.00 4.47 47.64 48.35
1982.
0 1.0 62 0.33 16.81 3.80 44.8 -0.01 103.60 4.34 41.92 48.59 19
81.0 1.0 122 0.65 17.46 3.33 30.9 -0.51 111.10 4.47 47.64 49.29
1980.
5 1.5 191 1.01 18.47 3.57 100.5 -0.48 141.80 4.61 54.20 49.80 19
80.0 2.0 167 0.88 19.35 3.60 100.5 -0.69 141.80 4.56 51.92 48.83
1979.
0 2.0 114 0.60 19.95 4.50 85.3 -0.52 140.50 4.45 46.87 50.17 19
78.5 2.5 147 0.78 20.73 4.30 37.7 -0.08 139.60 4.52 50.01 51.43
1977.
5 2.5 131 0.69 21.43 4.20 22.4 -0.40 92.50 4.48 48.49 51.09 19
77.0 3.0 151 0.80 22.22 4.20 22.4 -0.26 104.00 4.52 50.40 50.71
1976.
0 3.0 139 0.74 22.96 4.10 44.2 -0.91 152.30 4.50 49.25 49.55 19
75.5 3.5 262 1.39 24.35 4.60 76.3 -0.05 128.00 4.75 60.96 49.09
1975.
0 4.0 195 1.03 25.38 4.60 76.3 -0.27 179.00 4.62 54.58 48.63 19
74.0 4.0 86 0.46 25.83 4.10 37 -0.52 158.00 4.39 44.21 48.03
1973.
0 4.0 151 0.80 26.63 5.10 29 -0.54 170.00 4.52 50.40 47.09 19
72.0 4.0 45 0.24 26.87 4.10 58 -0.89 115.00 4.31 40.31 46.15
1971.
0 4.0 66 0.35 27.22 5.10 114 -0.40 118.00 4.35 42.30 44.43 19
70.0 4.0 98 0.52 27.74 4.87 58 130.00 4.42 45.35 43.18
1969.
0 4.0 68 0.36 28.10 3.87 66 121.00 4.35 42.49 43.06 19
68.0 4.0 53 0.28 28.38 3.80 25 172.00 4.32 41.07 42.09
1967.
0 4.0 40 0.21 28.59 3.07 56 109.00 4.30 39.83 42.39 19
66.0 4.0 81 0.43 29.02 3.77 87 100.00 4.38 43.73 43.35
1965.
0 4.0 64 0.34 29.36 4.03 51 178.00 4.35 42.11 43.48 19
64.5 4.5 73 0.39 29.74 4.00 30 102.70 4.36 42.97 43.41
1964.
0 5.0 49 0.26 30.00 4.00 30 102.70 4.31 40.69 43.80 19
63.0 5.0 77 0.41 30.41 3.50 44 149.00 4.37 43.35 43.91
1962.
5 5.5 167 0.88 31.29 3.63 52 177.00 4.56 51.92 44.07
19 5.5 111 0.59 31.88 3.00 45 188.00 4.44 46.59 44.08
78
61.5
1960.
5 5.5 61 0.32 32.20 5.27 45 188.00 4.34 41.83 43.86 19
59.5 5.5 94 0.50 32.70 4.70 46 250.00 4.41 44.97 44.43
1958.
5 5.5 52 0.28 32.98 3.90 51 97.60 4.32 40.97 44.27 19
57.5 5.5 97 0.51 33.49 3.90 72 127.90 4.41 45.26 43.58
1956.
5 5.5 66 0.35 33.84 4.60 34 95.60 4.35 42.30 43.49 19
55.5 5.5 49 0.26 34.10 4.20 32.2 91.80 4.31 40.69 43.92
1955.
0 6.0 109 0.58 34.68 4.20 32.2 91.80 4.44 46.40 44.15 19
54.0 6.0 61 0.32 35.00 3.60 56.6 201.70 4.34 41.83 44.87
1953.
0 6.0 94 0.50 35.50 4.40 46.4 107.10 4.41 44.97 44.60 19
52.5 6.5 102 0.54 36.04 5.50 56.9 98.20 4.42 45.73 44.60
1951.
5 6.5 106 0.56 36.60 4.70 43.2 110.90 4.43 46.11 45.26 19
50.5 6.5 118 0.62 37.22 4.30 33.1 96.40 4.46 47.25 45.02
1949.
5 6.5 127 0.67 37.89 4.50 34 80.90 4.48 48.11 44.97 19
48.5 6.5 69 0.37 38.26 3.30 29.1 79.90 4.36 42.59 44.49
1947.
5 6.5 66 0.35 38.61 3.63 28.8 90.00 4.35 42.30 44.02 19
46.5 6.5 118 0.62 39.23 4.00 56.9 181.00 4.46 47.25 45.45
1945.
5 6.5 84 0.44 39.68 4.40 24.3 62.10 4.39 44.02 45.01 19
45.0 7.0 56 0.30 39.97 4.40 24.3 62.10 4.33 41.35 44.67
1944.
5 7.5 44 0.23 40.21 3.87 4.30 40.21 44.63 19
43.5 7.5 52 0.28 40.48 3.70 4.32 40.97 44.57
1942.
5 7.5 256 1.35 41.84 3.87 4.74 60.39 44.13 19
41.5 7.5 72 0.38 42.22 4.00 37.4 155.70 4.36 42.88 44.25
1940.
5 7.5 92 0.49 42.70 3.97 65.7 140.30 4.40 44.78 44.47 19
39.5 7.5 64 0.34 43.04 4.03 60.1 104.30 4.35 42.11 44.47
1939.
0 8.0 60 0.32 43.36 4.00 60.1 112.60 4.34 41.73 46.26 19
38.5 8.5 72 0.38 43.74 4.20 42.9 194.00 4.36 42.88 45.31
1938.
0 9.0 96 0.51 44.25 4.20 42.9 123.00 4.41 45.16 45.24 19
37.5 9.5 80 0.42 44.67 4.90 99.4 134.00 4.38 43.64 44.70
1936. 9.5 44 0.23 44.90 4.53 46.2 113.00 4.30 40.21 44.47
79
5
1935.
5 9.5 240 1.27 46.17 4.17 49.8 104.90 4.71 58.87 44.17 19
35.0 10.0 156 0.83 47.00 4.20 49.8 112.50 4.54 50.87 43.98
1934.
5 10.5 64 0.34 47.34 5.00 14 177.60 4.35 42.11 43.37 19
33.5 10.5 36 0.19 47.53 5.10 59 77.80 4.29 39.45 43.37
1933.
0 11.0 40 0.21 47.74 5.10 59 96.40 4.30 39.83 43.37 19
32.0 11.0 28 0.15 47.89 4.27 31 75.70 4.27 38.69 41.66
1931.
0 11.0 52 0.28 48.16 4.27 35 108.10 4.32 40.97 40.71 19
30.5 11.5 32 0.17 48.33 4.80 26.4 108.80 4.28 39.07 40.51
1929.
5 11.5 80 0.42 48.76 5.60 22.3 206.60 4.38 43.64 40.48 19
29.0 12.0 44 0.23 48.99 5.60 22.3 146.80 4.30 40.21 41.16
1928.
0 12.0 60 0.32 49.31 3.03 14.8 109.90 4.34 41.73 41.24 19
27.0 12.0 56 0.30 49.60 3.83 35.8 68.80 4.33 41.35 41.77
1926.
5 12.5 44 0.23 49.84 4.33 20.1 82.10 4.30 40.21 42.15 19
26.0 13.0 32 0.17 50.01 4.30 20.1 115.70 4.28 39.07 42.61
1925.
0 13.0 112 0.59 50.60 3.83 19.6 98.00 4.44 46.68 43.22 19
24.0 13.0 36 0.19 50.79 5.13 33.1 94.20 4.29 39.45 43.22
1923.
0 13.0 108 0.57 51.36 4.93 18.2 95.10 4.44 46.30 43.45 19
22.0 13.0 72 0.38 51.74 4.77 26.3 138.30 4.36 42.88 43.83
1921.
0 13.0 128 0.68 52.42 6.07 37.4 82.90 4.48 48.21 44.25 19
20.0 13.0 108 0.57 52.99 5.07 21.7 133.00 4.44 46.30 43.64
1919.
0 13.0 60 0.32 53.31 4.07 72 167.90 4.34 41.73 44.28 19
18.0 13.0 80 0.42 53.73 4.57 18 144.70 4.38 43.64 43.98
1917.
0 13.0 84 0.44 54.18 5.10 19.2 153.00 4.39 44.02 43.98 19
16.0 13.0 76 0.40 54.58 2.47 44 150.10 4.37 43.26 44.44
1915.
5 13.5 48 0.25 54.83 3.87 31.4 78.60 4.31 40.59 44.21 19
14.5 13.5 104 0.55 55.38 3.20 29.2 112.30 4.43 45.92 45.20
1913.
5 13.5 76 0.40 55.78 4.00 32.7 135.40 4.37 43.26 45.01 19
12.5 13.5 72 0.38 56.16 3.50 35.3 189.90 4.36 42.88 44.51
1911.
5 13.5 176 0.93 57.10 4.58 52.78 44.36
80
1910.
5 13.5 84 0.44 57.54 4.39 44.02 44.59 19
09.5 13.5 164 0.87 58.41 4.55 51.63 44.47
1908.
5 13.5 60 0.32 58.73 4.34 41.73 44.44 19
07.5 13.5 32 0.17 58.90 4.28 39.07 43.98
1906.
5 13.5 60 0.32 59.21 4.34 41.73 43.26 19
05.5 13.5 72 0.38 59.59 4.36 42.88 43.10
1904.
5 13.5 92 0.49 60.08 4.40 44.78 41.89 19
03.5 13.5 72 0.38 60.46 4.36 42.88 41.70
1902.
5 13.5 24 0.13 60.59 4.26 38.31 41.81 19
01.5 13.5 100 0.53 61.12 4.42 45.54 41.62
1900.
5 13.5 68 0.36 61.48 4.35 42.49 41.20 18
99.5 13.5 36 0.19 61.67 4.29 39.45 41.31
1898.
5 13.5 40 0.21 61.88 4.30 39.83 41.35 18
97.5 13.5 44 0.23 62.11 4.30 40.21 41.54
1896.
5 13.5 40 0.21 62.32 4.30 39.83 41.62 18
95.5 13.5 28 0.15 62.47 4.27 38.69 41.39
1894.
5 13.5 104 0.55 63.02 4.43 45.92 41.89 18
93.5 13.5 76 0.40 63.42 4.37 43.26 41.81
1892.
5 13.5 44 0.23 63.66 4.30 40.21 41.89 18
91.5 13.5 108 0.57 64.23 4.44 46.30 41.85
1890.
5 13.5 44 0.23 64.46 4.30 40.21 42.34 18
89.5 13.5 88 0.47 64.93 4.40 44.40 42.72
1888.
5 13.5 32 0.17 65.10 4.28 39.07 42.61 18
87.5 13.5 52 0.28 65.37 4.32 40.97 43.71
1886.
5 13.5 36 0.19 65.56 4.29 39.45 43.33 18
85.5 13.5 80 0.42 65.99 4.38 43.64 43.48
1884.
5 13.5 144 0.76 66.75 4.51 49.73 43.56 18
83.5 13.5 64 0.34 67.09 4.35 42.11 43.90
1882.
5 13.5 160 0.85 67.93 4.54 51.25 43.75
18 13.5 68 0.36 68.29 4.35 42.49 43.75
81
81.5
1880.
5 13.5 60 0.32 68.61 4.34 41.73 43.52 18
79.5 13.5 96 0.51 69.12 4.41 45.16 42.76
1878.
5 13.5 68 0.36 69.48 4.35 42.49 42.49 18
77.5 13.5 36 0.19 69.67 4.29 39.45 42.80
1876.
5 13.5 36 0.19 69.86 4.29 39.45 42.46 18
75.5 13.5 56 0.30 70.16 4.33 41.35 42.19
1874.
5 13.5 64 0.34 70.49 4.35 42.11 41.58 18
73.5 13.5 36 0.19 70.68 4.29 39.45 41.70
1872.
5 13.5 192 1.02 71.70 4.61 54.30 42.65 18
71.5 13.5 32 0.17 71.87 4.28 39.07 43.18
1870.
5 13.5 32 0.17 72.04 4.28 39.07 43.45 18
69.5 13.5 32 0.17 72.21 4.28 39.07 43.64
1868.
5 13.5 80 0.42 72.63 4.38 43.64 43.64 18
67.5 13.5 136 0.72 73.35 4.49 48.97 42.19
1866.
5 13.5 92 0.49 73.84 4.40 44.78 42.91 18
65.5 13.5 84 0.44 74.28 4.39 44.02 43.10
1864.
5 13.5 84 0.44 74.73 4.39 44.02 43.56 18
63.5 13.5 36 0.19 74.92 4.29 39.45 43.22
1862.
5 13.5 40 0.21 75.13 4.30 39.83 42.84 18
61.5 13.5 108 0.57 75.70 4.44 46.30 42.80
1860.
5 13.5 52 0.28 75.98 4.32 40.97 42.72 18
59.5 13.5 80 0.42 76.40 4.38 43.64 43.60
1858.
5 13.5 44 0.23 76.63 4.30 40.21 45.08 18
57.5 13.5 96 0.51 77.14 4.41 45.16 45.08
1856.
5 13.5 88 0.47 77.61 4.40 44.40 44.44 18
55.5 13.5 76 0.40 78.01 4.37 43.26 44.17
1854.
5 13.5 176 0.93 78.94 4.58 52.78 43.60 18
53.5 13.5 192 1.02 79.96 4.61 54.30 43.33
1852. 13.5 40 0.21 80.17 4.30 39.83 42.57
82
5
1851.
5 13.5 40 0.21 80.38 4.30 39.83 42.91 18
50.5 13.5 24 0.13 80.51 4.26 38.31 43.03
1849.
5 13.5 20 0.11 80.61 4.26 37.93 41.77 18
48.5 13.5 16 0.08 80.70 4.25 37.55 40.78
1847.
5 13.5 16 0.08 80.78 4.25 37.55 40.86 18
46.5 13.5 124 0.66 81.44 4.47 47.83 40.67
1845.
5 13.5 88 0.47 81.90 4.40 44.40 41.09 18
45.0 14.0 44 0.23 82.14 4.30 40.21 41.73
1844.
5 14.5 88 0.47 82.60 4.40 44.40 42.30 18
44.0 15.0 48 0.25 82.86 4.31 40.59 43.03
1843.
5 15.5 20 0.11 82.96 4.26 37.93 42.15 18
42.5 15.5 68 0.36 83.32 4.35 42.49 41.85
1841.
5 15.5 88 0.47 83.79 4.40 44.40 42.23 18
40.5 15.5 76 0.40 84.19 4.37 43.26 42.00
1839.
5 15.5 92 0.49 84.68 4.40 44.78 41.85 18
38.5 15.5 32 0.17 84.84 4.28 39.07 42.19
1837.
5 15.5 56 0.30 85.14 4.33 41.35 41.96 18
36.5 15.5 84 0.44 85.59 4.39 44.02 41.43
1835.
5 15.5 64 0.34 85.92 4.35 42.11 40.93 18
34.5 15.5 32 0.17 86.09 4.28 39.07 40.71
1833.
5 15.5 56 0.30 86.39 4.33 41.35 40.55 18
32.5 15.5 44 0.23 86.62 4.30 40.21 40.36
1831.
5 15.5 32 0.17 86.79 4.28 39.07 39.91 18
30.5 15.5 24 0.13 86.92 4.26 38.31 39.79
1829.
5 15.5 68 0.36 87.28 4.35 42.49 40.10 18
28.5 15.5 16 0.08 87.36 4.25 37.55 40.13
1827.
5 15.5 36 0.19 87.55 4.29 39.45 40.59 18
26.5 15.5 36 0.19 87.74 4.29 39.45 40.55
1825.
5 15.5 52 0.28 88.02 4.32 40.97 40.59
83
1824.
5 15.5 64 0.34 88.36 4.35 42.11 40.67 18
23.5 15.5 60 0.32 88.68 4.34 41.73 41.16
1822.
5 15.5 92 0.49 89.16 4.40 44.78 41.05 18
21.5 15.5 28 0.15 89.31 4.27 38.69 40.83
1820.
5 15.5 28 0.15 89.46 4.27 38.69 40.56 18
19.5 15.5 76 0.40 89.86 4.37 43.26 40.56
1818.
5 15.5 68 0.36 90.22 4.35 42.49 41.17 18
17.5 15.5 24 0.13 90.35 4.26 38.31 40.60
1816.
5 15.5 13 0.07 90.42 4.24 37.26 41.40 18
15.5 15.5 24 0.13 90.54 4.26 38.31 41.51
1814.
5 15.5 64 0.34 90.88 4.35 42.11 40.98 18
14.0 16.0 124 0.66 91.54 4.47 47.83 40.71
1813.
0 16.0 32 0.17 91.71 4.28 39.07 40.68 18
12.0 16.0 112 0.59 92.30 4.44 46.68 41.05
1811.
0 16.0 40 0.21 92.51 4.30 39.83 41.31 18
10.0 16.0 20 0.11 92.62 4.26 37.93 41.35
1809.
0 16.0 40 0.21 92.83 4.30 39.83 40.40 18
08.0 16.0 20 0.11 92.94 4.26 37.93 40.63
1807.
0 16.0 52 0.28 93.21 4.32 40.97 39.91 18
06.0 16.0 52 0.28 93.49 4.32 40.97 40.93
1805.
0 16.0 68 0.36 93.85 4.35 42.49 40.97 18
04.0 16.0 24 0.13 93.97 4.26 38.31 41.50
1803.
0 16.0 56 0.30 94.27 4.33 41.35 41.62 18
02.0 16.0 36 0.19 94.46 4.29 39.45 42.23
1801.
0 16.0 148 0.78 95.24 4.52 50.11 41.96 18
00.0 16.0 24 0.13 95.37 4.26 38.31 41.66
1799.
0 16.0 96 0.51 95.88 4.41 45.16 41.62 17
98.0 16.0 32 0.17 96.05 4.28 39.07 41.70
1797.
0 16.0 116 0.61 96.66 4.45 47.06 42.30
17 16.0 24 0.13 96.79 4.26 38.31 41.85
84
96.0
1795.
0 16.0 36 0.19 96.98 4.29 39.45 41.89 17
94.0 16.0 20 0.11 97.08 4.26 37.93 41.50
1793.
0 16.0 64 0.34 97.42 4.35 42.11 41.77 17
92.0 16.0 100 0.53 97.95 4.42 45.54 41.58
1791.
0 16.0 100 0.53 98.48 4.42 45.54 42.38 17
90.0 16.0 28 0.15 98.63 4.27 38.69 42.32
1789.
0 16.0 56 0.30 98.93 4.33 41.35 42.88 17
88.0 16.0 60 0.32 99.24 4.34 41.73 42.61
1787.
5 16.5 96 0.51 99.75 4.41 45.16 42.11 17
86.5 16.5 108 0.57
100.32 4.44 46.30 41.85
1785.
5 16.5 30 0.16 100.4
8 4.28 38.88 42.32 17
84.5 16.5 78 0.41
100.89 4.37 43.45 42.25
1783.
5 16.5 36 0.19 101.0
8 4.29 39.45 42.08 17
82.5 16.5 48 0.25
101.34 4.31 40.59 41.90
1781.
5 16.5 72 0.38 101.7
2 4.36 42.88 41.28 17
80.5 16.5 78 0.41
102.13 4.37 43.45 41.22
1779.
5 16.5 48 0.25 102.3
9 4.31 40.59 41.33 17
78.5 16.5 42 0.22
102.61 4.30 40.02 41.45
1777.
5 16.5 78 0.41 103.0
2 4.37 43.45 41.33 17
76.5 16.5 42 0.22
103.24 4.30 40.02 41.16
1775.
5 16.5 24 0.13 103.3
7 4.26 38.31 40.88 17
74.5 16.5 90 0.48
103.85 4.40 44.59 40.99
1773.
5 16.5 48 0.25 104.1
0 4.31 40.59 41.22 17
72.5 16.5 36 0.19
104.29 4.29 39.45 40.88
1771.
5 16.5 54 0.29 104.5
8 4.33 41.16 42.02 17
70.5 16.5 48 0.25
104.83 4.31 40.59 42.65
1769.
5 16.5 60 0.32 105.1
5 4.34 41.73 42.48 17
68.5 16.5 66 0.35
105.50 4.35 42.30 42.53
1767. 16.5 42 0.22
105.72 4.30 40.02 42.70
85
5
1766.
5 16.5 162 0.86 106.5
8 4.55 51.44 43.73 17
65.5 16.5 90 0.48
107.05 4.40 44.59 44.82
1764.
5 16.5 72 0.38 107.4
3 4.36 42.88 46.08 17
63.5 16.5 54 0.29
107.72 4.33 41.16 46.72
1762.
5 16.5 54 0.29 108.0
1 4.33 41.16 46.78 17
61.5 16.5 162 0.86
108.86 4.55 51.44 45.92
1760.
5 16.5 162 0.86 109.7
2 4.55 51.44 45.46 17
59.5 16.5 193 1.02
110.74 4.61 54.39 45.41
1758.
5 16.5 133 0.70 111.4
5 4.49 48.68 46.09 17
57.5 16.5 48 0.25
111.70 4.31 40.59 46.09
1756.
5 16.5 72 0.38 112.0
8 4.36 42.88 44.89 17
55.5 16.5 42 0.22
112.30 4.30 40.02 43.87
1754.
5 16.5 66 0.35 112.6
5 4.35 42.30 42.71 17
53.5 16.5 126 0.67
113.32 4.47 48.02 41.90
1752.
5 16.5 54 0.29 113.6
0 4.33 41.16 41.96 17
51.5 16.5 36 0.19
113.80 4.29 39.45 41.62
1750.
5 16.5 54 0.29 114.0
8 4.33 41.16 41.46 17
49.5 16.5 72 0.38
114.46 4.36 42.88 41.63
1748.
5 16.5 48 0.25 114.7
2 4.31 40.59 41.11 17
47.5 16.5 54 0.29
115.00 4.33 41.16 40.89
1746.
5 16.5 36 0.19 115.1
9 4.29 39.45 41.34 17
45.5 16.5 25 0.13
115.32 4.27 38.40 41.17
1744.
5 16.5 84 0.44 115.7
7 4.39 44.02 40.94 17
43.5 16.5 72 0.38
116.15 4.36 42.88 41.23
1742.
5 16.5 30 0.16 116.3
1 4.28 38.88 41.06 17
41.5 16.5 84 0.44
116.75 4.39 44.02 41.17
1740.
5 16.5 36 0.19 116.9
4 4.29 39.45 41.68 17
39.5 16.5 48 0.25
117.20 4.31 40.59 41.22
1738.
5 16.5 78 0.41 117.6
1 4.37 43.45 41.45
86
1737.
5 16.5 36 0.19 117.8
0 4.29 39.45 41.68 17
36.5 16.5 48 0.25
118.05 4.31 40.59 41.05
1735.
5 16.5 78 0.41 118.4
7 4.37 43.45 41.05 17
34.5 16.5 36 0.19
118.66 4.29 39.45 41.39
1733.
5 16.5 96 0.51 119.1
7 4.41 45.16 40.88 17
32.5 16.5 54 0.29
119.45 4.33 41.16 41.80
1731.
5 16.5 18 0.10 119.5
5 4.25 37.74 42.14 17
30.5 16.5 36 0.19
119.74 4.29 39.45 42.04
1729.
5 16.5 84 0.44 120.1
8 4.39 44.02 42.14 17
28.5 16.5 24 0.13
120.31 4.26 38.31 41.69
1727.
5 16.5 133 0.70 121.0
1 4.49 48.68 42.02 17
26.5 16.5 84 0.44
121.46 4.39 44.02 42.23
1725.
5 16.5 67 0.35 121.8
1 4.35 42.40 42.38 17
24.5 16.5 47 0.25
122.06 4.31 40.50 41.87
1723.
5 16.5 48 0.25 122.3
1 4.31 40.59 42.66 17
22.5 16.5 89 0.47
122.79 4.40 44.49 41.98
1721.
5 16.5 40 0.21 123.0
0 4.30 39.83 41.47 17
20.5 16.5 52 0.28
123.27 4.32 40.97 41.05
1719.
5 16.5 30 0.16 123.4
3 4.28 38.88 40.91 17
18.5 16.5 107 0.57
124.00 4.43 46.21 40.98
1717.
5 16.5 62 0.33 124.3
3 4.34 41.92 40.54 17
16.5 16.5 30 0.16
124.48 4.28 38.88 40.68
1715.
5 16.5 23 0.12 124.6
1 4.26 38.21 40.40 17
14.5 16.5 32 0.17
124.78 4.28 39.07 40.41
1713.
5 16.5 56 0.30 125.0
7 4.33 41.35 40.08 17
12.5 16.5 43 0.23
125.30 4.30 40.12 40.07
1711.
5 16.5 54 0.29 125.5
8 4.33 41.16 40.04 17
10.5 16.5 23 0.12
125.71 4.26 38.21 40.35
1710.
0 17.0 31 0.16 125.8
7 4.28 38.97 40.62
17 17.0 72 0.38 126.2 4.36 42.88 40.66
87
09.0
5
1708.
0 17.0 61 0.32 126.5
7 4.34 41.83 40.78 17
07.0 17.0 27 0.14
126.72 4.27 38.59 40.53
1706.
0 17.0 56 0.30 127.0
1 4.33 41.35 41.15 17
05.0 17.0 60 0.32
127.33 4.34 41.73 41.12
1704.
0 17.0 60 0.32 127.6
5 4.34 41.73 41.20 17
03.5 17.5 56 0.30
127.94 4.33 41.35 41.11
1702.
5 17.5 28 0.15 128.0
9 4.27 38.69 41.39 17
01.5 17.5 88 0.47
128.56 4.40 44.40 41.43
1700.
5 17.5 28 0.15 128.7
1 4.27 38.69 41.35 16
99.5 17.5 80 0.42
129.13 4.38 43.64 41.09
1698.
5 17.5 52 0.28 129.4
1 4.32 40.97 40.86 16
97.5 17.5 56 0.30
129.70 4.33 41.35 40.93
1696.
5 17.5 60 0.32 130.0
2 4.34 41.73 40.48 16
95.5 17.5 52 0.28
130.29 4.32 40.97 40.67
1694.
5 17.5 32 0.17 130.4
6 4.28 39.07 40.29 16
93.5 17.5 32 0.17
130.63 4.28 39.07 40.29
1692.
5 17.5 36 0.19 130.8
2 4.29 39.45 40.06 16
91.5 17.5 40 0.21
131.04 4.30 39.83 40.13
1690.
5 17.5 48 0.25 131.2
9 4.31 40.59 40.13 16
89.5 17.5 40 0.21
131.50 4.30 39.83 40.74
1688.
5 17.5 52 0.28 131.7
8 4.32 40.97 41.89 16
87.5 17.5 32 0.17
131.95 4.28 39.07 42.61
1686.
5 17.5 68 0.36 132.3
1 4.35 42.49 42.37 16
85.5 17.5 52 0.28
132.58 4.32 40.97 42.29
1684.
5 17.5 96 0.51 133.0
9 4.41 45.16 42.85 16
83.5 17.5 152 0.80
133.89 4.53 50.49 43.52
1682.
5 17.5 112 0.59 134.4
9 4.44 46.68 43.39 16
81.5 17.5 15 0.08
134.56 4.24 37.45 43.94
1680. 17.5 39 0.21
134.77 4.29 39.73 43.62
88
5
1679.
5 17.5 99 0.52 135.2
9 4.42 45.45 43.79 16
78.5 17.5 123 0.65
135.95 4.47 47.73 43.11
1677.
5 17.5 18 0.10 136.0
4 4.25 37.74 42.28 16
76.5 17.5 126 0.67
136.71 4.47 48.02 42.50
1675.
5 17.5 18 0.10 136.8
0 4.25 37.74 42.48 16
74.5 17.5 114 0.60
137.41 4.45 46.87 42.02
1673.
5 17.5 81 0.43 137.8
3 4.38 43.73 41.08 16
72.5 17.5 24 0.13
137.96 4.26 38.31 41.22
1671.
5 17.5 39 0.21 138.1
7 4.29 39.73 40.51 16
70.5 17.5 36 0.19
138.36 4.29 39.45 40.62
1669.
5 17.5 51 0.27 138.6
3 4.32 40.88 39.76 16
68.5 17.5 24 0.13
138.76 4.26 38.31 39.39
1667.
5 17.5 33 0.17 138.9
3 4.28 39.16 39.65 16
66.5 17.5 51 0.27
139.20 4.32 40.88 39.76
1665.
5 17.5 30 0.16 139.3
6 4.28 38.88 39.73 16
64.5 17.5 24 0.13
139.49 4.26 38.31 39.51
1663.
5 17.5 42 0.22 139.7
1 4.30 40.02 39.53 16
62.5 17.5 51 0.27
139.98 4.32 40.88 39.65
1661.
5 17.5 51 0.27 140.2
5 4.32 40.88 40.42 16
60.5 17.5 33 0.17
140.42 4.28 39.16 40.53
1659.
5 17.5 27 0.14 140.5
7 4.27 38.59 40.62 16
58.5 17.5 27 0.14
140.71 4.27 38.59 40.39
1658.
0 18.0 45 0.24 140.9
5 4.31 40.31 40.11 16
57.0 18.0 132 0.70
141.64 4.49 48.59 39.85
1656.
0 18.0 42 0.22 141.8
7 4.30 40.02 39.79 16
55.0 18.0 33 0.17
142.04 4.28 39.16 39.88
1654.
0 18.0 18 0.10 142.1
4 4.25 37.74 40.28 16
53.0 18.0 21 0.11
142.25 4.26 38.02 40.08
1652.
0 18.0 24 0.13 142.3
7 4.26 38.31 39.13
89
1651.
0 18.0 27 0.14 142.5
2 4.27 38.59 39.05 16
50.0 18.0 36 0.19
142.71 4.29 39.45 39.28
1649.
0 18.0 69 0.37 143.0
7 4.36 42.59 39.48 16
48.0 18.0 24 0.13
143.20 4.26 38.31 40.08
1647.
0 18.0 33 0.17 143.3
7 4.28 39.16 40.31 16
46.0 18.0 33 0.17
143.55 4.28 39.16 40.36
1645.
0 18.0 57 0.30 143.8
5 4.33 41.45 40.73 16
44.0 18.0 39 0.21
144.06 4.29 39.73 40.68
1643.
0 18.0 84 0.44 144.5
0 4.39 44.02 40.71 16
42.0 18.0 48 0.25
144.76 4.31 40.59 40.53
1641.
0 18.0 33 0.17 144.9
3 4.28 39.16 40.53 16
40.0 18.0 75 0.40
145.33 4.37 43.16 40.53
1639.
0 18.0 63 0.33 145.6
6 4.34 42.02 40.62 16
38.0 18.0 27 0.14
145.80 4.27 38.59 40.08
1637.
0 18.0 15 0.08 145.8
8 4.24 37.45 39.85 16
36.0 18.0 33 0.17
146.06 4.28 39.16 39.99
1635.
0 18.0 57 0.30 146.3
6 4.33 41.45 39.73 16
34.0 18.0 48 0.25
146.61 4.31 40.59 39.48
1633.
0 18.0 27 0.14 146.7
6 4.27 38.59 40.02 16
32.0 18.0 24 0.13
146.88 4.26 38.31 41.39
1631.
0 18.0 48 0.25 147.1
4 4.31 40.59 41.79 16
30.0 18.0 48 0.25
147.39 4.31 40.59 41.59
1629.
0 18.0 36 0.19 147.5
8 4.29 39.45 41.33 16
28.0 18.0 84 0.44
148.03 4.39 44.02 41.65
1627.
0 18.0 159 0.84 148.8
7 4.54 51.16 42.02 16
26.0 18.0 75 0.40
149.26 4.37 43.16 42.08
1625.
0 18.0 36 0.19 149.4
5 4.29 39.45 42.10 16
24.0 18.0 21 0.11
149.57 4.26 38.02 42.62
1623.
0 18.0 60 0.32 149.8
8 4.34 41.73 42.02
16 18.0 63 0.33 150.2 4.34 42.02 40.76
90
22.0
2
1621.
0 18.0 54 0.29 150.5
0 4.33 41.16 40.62 16
20.0 18.0 51 0.27
150.77 4.32 40.88 40.59
1619.
0 18.0 90 0.48 151.2
5 4.40 44.59 41.05 16
18.0 18.0 21 0.11
151.36 4.26 38.02 40.93
1617.
0 18.0 27 0.14 151.5
0 4.27 38.59 40.88 16
16.0 18.0 60 0.32
151.82 4.34 41.73 41.25
1615.
0 18.0 33 0.17 151.9
9 4.28 39.16 41.28 16
14.0 18.0 69 0.37
152.36 4.36 42.59 40.91
1613.
0 18.0 48 0.25 152.6
1 4.31 40.59 41.13 16
12.0 18.0 57 0.30
152.92 4.33 41.45 41.90
1611.
0 18.0 93 0.49 153.4
1 4.41 44.87 41.65 16
10.0 18.0 54 0.29
153.69 4.33 41.16 42.05
1609.
0 18.0 51 0.27 153.9
6 4.32 40.88 41.82 16
08.0 18.0 45 0.24
154.20 4.31 40.31 42.02
1607.
0 18.0 108 0.57 154.7
7 4.44 46.30 42.13 16
06.5 18.5 33 0.17
154.95 4.28 39.16 41.73
1605.
5 18.5 75 0.40 155.3
4 4.37 43.16 41.99 16
04.5 18.5 45 0.24
155.58 4.31 40.31 42.16
1603.
5 18.5 69 0.37 155.9
5 4.36 42.59 42.13 16
02.5 18.5 69 0.37
156.31 4.36 42.59 41.33
1601.
5 18.5 51 0.27 156.5
8 4.32 40.88 41.56 16
00.5 18.5 81 0.43
157.01 4.38 43.73 41.39
1599.
5 18.5 69 0.37 157.3
8 4.36 42.59 42.10 15
98.5 18.5 42 0.22
157.60 4.30 40.02 42.33
1597.
5 18.5 24 0.13 157.7
3 4.26 38.31 41.88 15
96.5 18.5 57 0.30
158.03 4.33 41.45 42.05
1595.
5 18.5 57 0.30 158.3
3 4.33 41.45 41.90 15
95.0 19.0 120 0.63
158.96 4.46 47.44 41.65
1594. 19.0 93 0.49
159.46 4.41 44.87 41.96
91
0
1593.
0 19.0 21 0.11 159.5
7 4.26 38.02 42.05 15
92.0 19.0 69 0.37
159.93 4.36 42.59 42.19
1591.
0 19.0 66 0.35 160.2
8 4.35 42.30 42.53 15
90.0 19.0 42 0.22
160.50 4.30 40.02 42.56
1589.
0 19.0 75 0.40 160.9
0 4.37 43.16 42.13 15
88.0 19.0 33 0.17
161.08 4.28 39.16 42.39
1587.
0 19.0 72 0.38 161.4
6 4.36 42.88 41.96 15
86.0 19.0 93 0.49
161.95 4.41 44.87 41.96
1585.
0 19.0 123 0.65 162.6
0 4.47 47.73 42.05 15
84.0 19.0 48 0.25
162.85 4.31 40.59 41.82
1583.
0 19.0 48 0.25 163.1
1 4.31 40.59 42.33 15
82.0 19.0 24 0.13
163.23 4.26 38.31 42.22
1581.
0 19.0 66 0.35 163.5
8 4.35 42.30 41.76 15
80.0 19.0 51 0.27
163.85 4.32 40.88 40.88
1579.
0 19.0 51 0.27 164.1
2 4.32 40.88 41.56 15
78.0 19.0 87 0.46
164.58 4.39 44.30 41.28
1577.
0 19.0 60 0.32 164.9
0 4.34 41.73 41.42 15
76.0 19.0 45 0.24
165.14 4.31 40.31 41.62
1575.
0 19.0 30 0.16 165.3
0 4.28 38.88 41.42 15
74.0 19.0 120 0.63
165.93 4.46 47.44 41.16
1573.
0 19.0 18 0.10 166.0
3 4.25 37.74 40.99 15
72.0 19.0 39 0.21
166.23 4.29 39.73 40.79
1571.
0 19.0 87 0.46 166.6
9 4.39 44.30 40.93 15
70.0 19.0 30 0.16
166.85 4.28 38.88 41.16
1569.
0 19.0 24 0.13 166.9
8 4.26 38.31 40.42 15
68.0 19.0 69 0.37
167.35 4.36 42.59 40.85
1567.
0 19.0 39 0.21 167.5
5 4.29 39.73 41.16 15
66.0 19.0 60 0.32
167.87 4.34 41.73 41.19
1565.
0 19.0 54 0.29 168.1
6 4.33 41.16 41.25
92
1564.
0 19.0 42 0.22 168.3
8 4.30 40.02 42.02 15
63.0 19.0 63 0.33
168.71 4.34 42.02 41.85
1562.
0 19.0 72 0.38 169.0
9 4.36 42.88 41.93 15
61.0 19.0 90 0.48
169.57 4.40 44.59 41.76
1560.
0 19.0 36 0.19 169.7
6 4.29 39.45 41.45 15
59.0 19.0 105 0.56
170.31 4.43 46.02 41.59
1558.
0 19.0 51 0.27 170.5
8 4.32 40.88 41.42 15
57.0 19.0 48 0.25
170.84 4.31 40.59 41.05
1556.
0 19.0 42 0.22 171.0
6 4.30 40.02 40.59 15
55.0 19.0 21 0.11
171.17 4.26 38.02 40.85
1554.
0 19.0 57 0.30 171.4
7 4.33 41.45 40.39 15
53.0 19.0 45 0.24
171.71 4.31 40.31 40.59
1552.
0 19.0 33 0.17 171.8
9 4.28 39.16 40.71 15
51.0 19.0 42 0.22
172.11 4.30 40.02 41.05
1550.
0 19.0 63 0.33 172.4
4 4.34 42.02 41.19 15
49.0 19.0 57 0.30
172.74 4.33 41.45 41.05
1548.
0 19.0 72 0.38 173.1
2 4.36 42.88 41.25 15
47.0 19.0 60 0.32
173.44 4.34 41.73 41.73
1546.
0 19.0 78 0.41 173.8
5 4.37 43.45 41.96 15
45.0 19.0 36 0.19
174.04 4.29 39.45 42.02
1544.
0 19.0 42 0.22 174.2
7 4.30 40.02 41.70 15
43.0 19.0 66 0.35
174.62 4.35 42.30 41.36
1542.
0 19.0 84 0.44 175.0
6 4.39 44.02 41.28 15
41.0 19.0 66 0.35
175.41 4.35 42.30 41.13
1540.
0 19.0 69 0.37 175.7
8 4.36 42.59 41.05 15
39.0 19.0 24 0.13
175.90 4.26 38.31 41.36
1538.
0 19.0 36 0.19 176.0
9 4.29 39.45 41.08 15
37.0 19.0 51 0.27
176.36 4.32 40.88 41.27
1536.
0 19.0 63 0.33 176.7
0 4.34 42.02 41.02
15 19.0 27 0.14 176.8 4.27 38.59 41.01
93
35.0
4
1534.
0 19.0 75 0.40 177.2
4 4.37 43.16 41.05 15
33.5 19.5 36 0.19
177.43 4.29 39.45 40.93
1533.
0 20.0 104 0.55 177.9
8 4.43 45.92 41.21 15
32.0 20.0 40 0.21
178.19 4.30 39.83 41.45
1531.
0 20.0 68 0.36 178.5
5 4.35 42.49 41.72 15
30.0 20.0 28 0.15
178.70 4.27 38.69 41.73
1529.
0 20.0 24 0.13 178.8
2 4.26 38.31 42.08 15
28.0 20.0 80 0.42
179.25 4.38 43.64 41.85
1527.
0 20.0 88 0.47 179.7
1 4.40 44.40 41.73 15
26.0 20.0 56 0.30
180.01 4.33 41.35 41.77
1525.
0 20.0 76 0.40 180.4
1 4.37 43.26 42.42 15
24.0 20.0 72 0.38
180.79 4.36 42.88 42.61
1523.
5 20.5 80 0.42 181.2
1 4.38 43.64 42.15 15
22.5 20.5 28 0.15
181.36 4.27 38.69 41.66
1521.
5 20.5 72 0.38 181.7
4 4.36 42.88 41.58 15
20.5 20.5 96 0.51
182.25 4.41 45.16 41.28
1519.
5 20.5 44 0.23 182.4
8 4.30 40.21 42.08 15
18.5 20.5 32 0.17
182.65 4.28 39.07 42.15
1517.
5 20.5 36 0.19 182.8
4 4.29 39.45 42.38 15
16.5 20.5 48 0.25
183.10 4.31 40.59 41.96
1515.
5 20.5 44 0.23 183.3
3 4.30 40.21 41.35 15
14.5 20.5 156 0.83
184.16 4.54 50.87 41.12
1513.
5 20.5 88 0.47 184.6
2 4.40 44.40 41.12 15
12.5 20.5 52 0.28
184.90 4.32 40.97 41.16
1511.
5 20.5 28 0.15 185.0
5 4.27 38.69 40.97 15
10.5 20.5 32 0.17
185.22 4.28 39.07 40.93
1509.
5 20.5 20 0.11 185.3
2 4.26 37.93 40.86 15
08.5 20.5 32 0.17
185.49 4.28 39.07 40.97
1507. 20.5 40 0.21
185.70 4.30 39.83 40.90
94
5
1506.
5 20.5 28 0.15 185.8
5 4.27 38.69 41.24 15
05.5 20.5 40 0.21
186.06 4.30 39.83 41.31
1504.
5 20.5 148 0.78 186.8
5 4.52 50.11 41.43 15
03.5 20.5 100 0.53
187.37 4.42 45.54 41.39
1502.
5 20.5 44 0.23 187.6
1 4.30 40.21 42.11 15
01.5 20.5 64 0.34
187.95 4.35 42.11 42.53
1500.
5 20.5 40 0.21 188.1
6 4.30 39.83 42.30 14
99.5 20.5 32 0.17
188.33 4.28 39.07 41.35
1498.
5 20.5 28 0.15 188.4
7 4.27 38.69 40.67 14
97.5 20.5 116 0.61
189.09 4.45 47.06 41.05
1496.
5 20.5 72 0.38 189.4
7 4.36 42.88 41.20 14
95.5 20.5 16 0.08
189.55 4.25 37.55 41.01
1494.
5 20.5 48 0.25 189.8
1 4.31 40.59 41.01 14
93.5 20.5 28 0.15
189.96 4.27 38.69 41.24
1492.
5 20.5 84 0.44 190.4
0 4.39 44.02 40.90 14
91.5 20.5 80 0.42
190.82 4.38 43.64 40.48
1490.
5 20.5 20 0.11 190.9
3 4.26 37.93 41.09 14
89.5 20.5 32 0.17
191.10 4.28 39.07 40.93
1488.
5 20.5 52 0.28 191.3
7 4.32 40.97 41.05 14
87.5 20.5 80 0.42
191.80 4.38 43.64 40.82
1486.
5 20.5 28 0.15 191.9
5 4.27 38.69 40.71 14
85.5 20.5 80 0.42
192.37 4.38 43.64 41.47
1484.
5 20.5 32 0.17 192.5
4 4.28 39.07 41.43 14
83.5 20.5 40 0.21
192.75 4.30 39.83 41.50
1482.
5 20.5 60 0.32 193.0
7 4.34 41.73 41.31 14
81.5 20.5 68 0.36
193.43 4.35 42.49 41.35
1480.
5 20.5 100 0.53 193.9
6 4.42 45.54 41.20 14
79.5 20.5 28 0.15
194.11 4.27 38.69 41.20
1478.
5 20.5 60 0.32 194.4
2 4.34 41.73 41.39
95
1477.
5 20.5 60 0.32 194.7
4 4.34 41.73 41.28 14
76.5 20.5 32 0.17
194.91 4.28 39.07 41.28
1475.
5 20.5 64 0.34 195.2
5 4.35 42.11 41.09 14
74.5 20.5 32 0.17
195.42 4.28 39.07 41.16
1473.
5 20.5 60 0.32 195.7
3 4.34 41.73 40.90 14
72.5 20.5 48 0.25
195.99 4.31 40.59 41.16
1471.
5 20.5 68 0.36 196.3
5 4.35 42.49 41.39 14
70.5 20.5 80 0.42
196.77 4.38 43.64 41.12
1469.
5 20.5 36 0.19 196.9
6 4.29 39.45 41.62 14
68.5 20.5 32 0.17
197.13 4.28 39.07 41.89
1467.
5 20.5 88 0.47 197.6
0 4.40 44.40 41.96 14
66.5 20.5 56 0.30
197.89 4.33 41.35 41.89
1465.
5 20.5 36 0.19 198.0
8 4.29 39.45 41.77 14
64.5 20.5 84 0.44
198.53 4.39 44.02 42.11
1463.
5 20.5 88 0.47 198.9
9 4.40 44.40 42.38 14
62.5 20.5 56 0.30
199.29 4.33 41.35 42.00
1461.
5 20.5 60 0.32 199.6
1 4.34 41.73 42.34 14
60.5 20.5 68 0.36
199.97 4.35 42.49 42.23
1459.
5 20.5 72 0.38 200.3
5 4.36 42.88 41.89 14
58.5 20.5 60 0.32
200.67 4.34 41.73 41.20
1457.
5 20.5 48 0.25 200.9
2 4.31 40.59 41.28 14
56.5 20.5 92 0.49
201.41 4.40 44.78 40.90
1455.
5 20.5 24 0.13 201.5
3 4.26 38.31 40.74 14
54.5 20.5 48 0.25
201.79 4.31 40.59 40.67
1453.
5 20.5 16 0.08 201.8
7 4.25 37.55 41.09 14
52.5 20.5 64 0.34
202.21 4.35 42.11 41.05
1451.
5 20.5 20 0.11 202.3
2 4.26 37.93 40.67 14
50.5 20.5 52 0.28
202.59 4.32 40.97 41.28
1449.
5 20.5 64 0.34 202.9
3 4.35 42.11 40.97
14 20.5 104 0.55 203.4 4.43 45.92 41.35
96
48.5
8
1447.
5 20.5 44 0.23 203.7
1 4.30 40.21 41.12 14
46.5 20.5 52 0.28
203.99 4.32 40.97 41.89
1445.
5 20.5 88 0.47 204.4
6 4.40 44.40 42.61 14
44.5 20.5 16 0.08
204.54 4.25 37.55 42.46
1443.
5 20.5 56 0.30 204.8
4 4.33 41.35 41.62 14
42.5 20.5 40 0.21
205.05 4.30 39.83 41.39
1441.
5 20.5 100 0.53 205.5
8 4.42 45.54 41.85 14
40.5 20.5 128 0.68
206.25 4.48 48.21 41.73
1439.
5 20.5 48 0.25 206.5
1 4.31 40.59 42.19 14
38.5 20.5 16 0.08
206.59 4.25 37.55 42.34
1437.
5 20.5 20 0.11 206.7
0 4.26 37.93 42.61 14
36.5 20.5 100 0.53
207.23 4.42 45.54 42.11
1435.
5 20.5 76 0.40 207.6
3 4.37 43.26 41.43 14
34.5 20.5 64 0.34
207.97 4.35 42.11 41.54
1433.
5 20.5 72 0.38 208.3
5 4.36 42.88 42.80 14
32.5 20.5 68 0.36
208.71 4.35 42.49 43.29
1431.
5 20.5 48 0.25 208.9
6 4.31 40.59 42.65 14
30.5 20.5 56 0.30
209.26 4.33 41.35 42.23
1429.
5 20.5 60 0.32 209.5
8 4.34 41.73 42.15 14
28.5 20.5 148 0.78
210.36 4.52 50.11 42.19
1427.
5 20.5 72 0.38 210.7
4 4.36 42.88 42.34 14
26.5 20.5 32 0.17
210.91 4.28 39.07 42.69
1425.
5 20.5 32 0.17 211.0
8 4.28 39.07 42.88 14
24.5 20.5 56 0.30
211.38 4.33 41.35 42.88
1423.
5 20.5 76 0.40 211.7
8 4.37 43.26 42.23 14
22.5 20.5 84 0.44
212.22 4.39 44.02 41.77
1421.
5 20.5 84 0.44 212.6
7 4.39 44.02 42.61 14
20.5 20.5 76 0.40
213.07 4.37 43.26 42.69
1419. 20.5 60 0.32
213.39 4.34 41.73 42.49
97
5
1418.
5 20.5 80 0.42 213.8
1 4.38 43.64 42.11 14
17.5 20.5 24 0.13
213.94 4.26 38.31 41.58
1416.
5 20.5 120 0.63 214.5
7 4.46 47.44 41.39 14
15.5 20.5 40 0.21
214.78 4.30 39.83 41.16
1414.
5 20.5 36 0.19 214.9
8 4.29 39.45 41.81 14
13.5 20.5 36 0.19
215.17 4.29 39.45 42.11
1412.
5 20.5 28 0.15 215.3
1 4.27 38.69 42.34 14
11.5 20.5 64 0.34
215.65 4.35 42.11 42.00
1410.
5 20.5 52 0.28 215.9
3 4.32 40.97 42.30 14
09.5 20.5 128 0.68
216.60 4.48 48.21 42.27
1408.
5 20.5 112 0.59 217.2
0 4.44 46.68 42.61 14
07.5 20.5 48 0.25
217.45 4.31 40.59 43.90
1406.
5 20.5 84 0.44 217.9
0 4.39 44.02 44.40 14
05.5 20.5 72 0.38
218.28 4.36 42.88 44.40
1404.
5 20.5 32 0.17 218.4
5 4.28 39.07 43.56 14
03.5 20.5 72 0.38
218.83 4.36 42.88 43.07
1402.
5 20.5 164 0.87 219.7
0 4.55 51.63 43.03 14
01.5 20.5 116 0.61
220.31 4.45 47.06 42.80
1400.
5 20.5 52 0.28 220.5
8 4.32 40.97 42.76 13
99.5 20.5 40 0.21
220.80 4.30 39.83 42.72
1398.
5 20.5 60 0.32 221.1
1 4.34 41.73 43.07 13
97.5 20.5 44 0.23
221.35 4.30 40.21 42.11
1396.
5 20.5 60 0.32 221.6
6 4.34 41.73 41.50 13
95.5 20.5 68 0.36
222.02 4.35 42.49 41.73
1394.
5 20.5 28 0.15 222.1
7 4.27 38.69 41.58 13
93.5 20.5 108 0.57
222.74 4.44 46.30 41.62
1392.
5 20.5 64 0.34 223.0
8 4.35 42.11 41.77 13
91.5 20.5 52 0.28
223.36 4.32 40.97 41.96
1390.
5 20.5 76 0.40 223.7
6 4.37 43.26 41.58
98
1389.
5 20.5 24 0.13 223.8
9 4.26 38.31 41.50 13
88.5 20.5 64 0.34
224.22 4.35 42.11 41.43
1387.
5 20.5 60 0.32 224.5
4 4.34 41.73 41.24 13
86.5 20.5 80 0.42
224.97 4.38 43.64 41.12
1385.
5 20.5 28 0.15 225.1
1 4.27 38.69 40.90 13
84.5 20.5 20 0.11
225.22 4.26 37.93 41.09
1383.
5 20.5 100 0.53 225.7
5 4.42 45.54 40.93 13
82.5 20.5 44 0.23
225.98 4.30 40.21 41.12
1381.
5 20.5 40 0.21 226.1
9 4.30 39.83 40.59 13
80.5 20.5 52 0.28
226.47 4.32 40.97 40.71
1379.
5 20.5 44 0.23 226.7
0 4.30 40.21 41.58 13
78.5 20.5 48 0.25
226.96 4.31 40.59 40.93
1377.
5 20.5 80 0.42 227.3
8 4.38 43.64 41.47 13
76.5 20.5 24 0.13
227.51 4.26 38.31 41.47
1375.
5 20.5 40 0.21 227.7
2 4.30 39.83 41.62 13
74.5 20.5 112 0.59
228.31 4.44 46.68 41.81
1373.
5 20.5 32 0.17 228.4
8 4.28 39.07 41.70 13
72.5 20.5 100 0.53
229.01 4.42 45.54 41.35
1371.
5 20.5 40 0.21 229.2
2 4.30 39.83 41.62 13
70.5 20.5 68 0.36
229.58 4.35 42.49 42.19
1369.
5 20.5 64 0.34 229.9
2 4.35 42.11 41.39 13
68.5 20.5 36 0.19
230.11 4.29 39.45 42.23
1367.
5 20.5 44 0.23 230.3
4 4.30 40.21 41.73 13
66.5 20.5 52 0.28
230.62 4.32 40.97 42.19
1365.
5 20.5 100 0.53 231.1
5 4.42 45.54 41.92 13
65.0 21.0 28 0.15
231.29 4.27 38.69 41.73
1364.
0 21.0 120 0.63 231.9
3 4.46 47.44 41.73 13
63.0 21.0 48 0.25
232.18 4.31 40.59 41.77
1362.
0 21.0 88 0.47 232.6
5 4.40 44.40 41.70
13 21.0 40 0.21 232.8 4.30 39.83 41.01
99
61.0
6
1360.
0 21.0 44 0.23 233.0
9 4.30 40.21 41.20 13
59.0 21.0 36 0.19
233.28 4.29 39.45 40.55
1358.
0 21.0 48 0.25 233.5
4 4.31 40.59 40.40 13
57.0 21.0 44 0.23
233.77 4.30 40.21 40.25
1356.
0 21.0 28 0.15 233.9
2 4.27 38.69 40.25 13
55.0 21.0 48 0.25
234.17 4.31 40.59 40.13
1354.
0 21.0 52 0.28 234.4
5 4.32 40.97 40.74 13
53.0 21.0 32 0.17
234.62 4.28 39.07 40.63
1352.
0 21.0 72 0.38 235.0
0 4.36 42.88 40.63 13
51.0 21.0 40 0.21
235.21 4.30 39.83 40.67
1350.
0 21.0 32 0.17 235.3
8 4.28 39.07 41.05 13
49.0 21.0 100 0.53
235.91 4.42 45.54 41.24
1348.
0 21.0 36 0.19 236.1
0 4.29 39.45 41.09 13
47.0 21.0 44 0.23
236.33 4.30 40.21 40.71
1346.
0 21.0 32 0.17 236.5
0 4.28 39.07 40.74 13
45.0 21.0 88 0.47
236.97 4.40 44.40 41.92
1344.
0 21.0 72 0.38 237.3
5 4.36 42.88 41.47 13
43.0 21.0 16 0.08
237.43 4.25 37.55 41.35
1342.
0 21.0 32 0.17 237.6
0 4.28 39.07 41.20 13
41.0 21.0 44 0.23
237.83 4.30 40.21 41.58
1340.
0 21.0 156 0.83 238.6
6 4.54 50.87 41.35 13
39.0 21.0 52 0.28
238.94 4.32 40.97 41.43
1338.
0 21.0 24 0.13 239.0
6 4.26 38.31 42.08 13
37.0 21.0 28 0.15
239.21 4.27 38.69 41.92
1336.
0 21.0 72 0.38 239.5
9 4.36 42.88 42.46 13
35.0 21.0 64 0.34
239.93 4.35 42.11 42.00
1334.
0 21.0 80 0.42 240.3
5 4.38 43.64 41.89 13
33.0 21.0 84 0.44
240.80 4.39 44.02 42.46
1332. 21.0 16 0.08
240.88 4.25 37.55 42.46
100
0
1331.
0 21.0 100 0.53 241.4
1 4.42 45.54 42.69 13
30.0 21.0 108 0.57
241.98 4.44 46.30 42.65
1329.
0 21.0 40 0.21 242.1
9 4.30 39.83 42.42 13
28.0 21.0 84 0.44
242.64 4.39 44.02 42.91
1327.
0 21.0 28 0.15 242.7
9 4.27 38.69 43.87 13
26.0 21.0 96 0.51
243.30 4.41 45.16 43.45
1325.
0 21.0 60 0.32 243.6
1 4.34 41.73 43.07 13
24.0 21.0 56 0.30
243.91 4.33 41.35 43.07
1323.
5 21.5 136 0.72 244.6
3 4.49 48.97 42.99 13
23.0 22.0 116 0.61
245.24 4.45 47.06 43.18
1322.
0 22.0 56 0.30 245.5
4 4.33 41.35 43.10 13
21.0 22.0 68 0.36
245.90 4.35 42.49 42.88
1320.
0 22.0 40 0.21 246.1
1 4.30 39.83 42.69 13
19.0 22.0 76 0.40
246.51 4.37 43.26 42.00
1318.
0 22.0 48 0.25 246.7
7 4.31 40.59 41.35 13
17.0 22.0 88 0.47
247.23 4.40 44.40 41.39
1316.
0 22.0 36 0.19 247.4
2 4.29 39.45 41.35 13
15.0 22.0 36 0.19
247.61 4.29 39.45 41.58
1314.
0 22.0 64 0.34 247.9
5 4.35 42.11 41.39 13
13.0 22.0 48 0.25
248.21 4.31 40.59 41.58
1312.
0 22.0 60 0.32 248.5
2 4.34 41.73 41.20 13
11.0 22.0 64 0.34
248.86 4.35 42.11 41.43
1310.
0 22.0 64 0.34 249.2
0 4.35 42.11 41.39 13
09.0 22.0 56 0.30
249.50 4.33 41.35 41.43
1308.
0 22.0 68 0.36 249.8
6 4.35 42.49 42.38 13
07.0 22.0 48 0.25
250.11 4.31 40.59 42.11
1306.
0 22.0 60 0.32 250.4
3 4.34 41.73 42.38 13
05.0 22.0 32 0.17
250.60 4.28 39.07 42.00
1304.
0 22.0 68 0.36 250.9
6 4.35 42.49 41.66
101
1303.
0 22.0 148 0.78 251.7
4 4.52 50.11 41.39 13
02.0 22.0 32 0.17
251.91 4.28 39.07 41.50
1301.
0 22.0 92 0.49 252.4
0 4.40 44.78 41.43 13
00.0 22.0 24 0.13
252.52 4.26 38.31 41.92
1299.
0 22.0 20 0.11 252.6
3 4.26 37.93 43.07 12
98.0 22.0 40 0.21
252.84 4.30 39.83 41.96
1297.
0 22.0 60 0.32 253.1
6 4.34 41.73 42.08 12
96.0 22.0 52 0.28
253.43 4.32 40.97 41.39
1295.
0 22.0 84 0.44 253.8
8 4.39 44.02 42.42 12
94.0 22.0 188 0.99
254.87 4.60 53.92 43.10
1293.
0 22.0 32 0.17 255.0
4 4.28 39.07 43.68 12
92.0 22.0 44 0.23
255.28 4.30 40.21 43.98
1291.
0 22.0 20 0.11 255.3
8 4.26 37.93 44.17 12
90.0 22.0 132 0.70
256.08 4.49 48.59 44.21
1289.
0 22.0 92 0.49 256.5
7 4.40 44.78 43.14 12
88.0 22.0 100 0.53
257.10 4.42 45.54 44.40
1287.
0 22.0 92 0.49 257.5
8 4.40 44.78 44.44 12
86.0 22.0 72 0.38
257.96 4.36 42.88 44.59
1285.
0 22.0 88 0.47 258.4
3 4.40 44.40 44.09 12
84.0 22.0 76 0.40
258.83 4.37 43.26 43.37
1283.
0 22.0 164 0.87 259.7
0 4.55 51.63 43.22 12
82.0 22.0 48 0.25
259.95 4.31 40.59 42.53
1281.
0 22.0 36 0.19 260.1
4 4.29 39.45 42.61 12
80.0 22.0 80 0.42
260.57 4.38 43.64 42.34
1279.
0 22.0 16 0.08 260.6
5 4.25 37.55 42.15 12
78.0 22.0 84 0.44
261.10 4.39 44.02 41.35
1277.
0 22.0 20 0.11 261.2
0 4.26 37.93 41.54 12
76.0 22.0 80 0.42
261.63 4.38 43.64 41.70
1275.
0 22.0 60 0.32 261.9
4 4.34 41.73 41.66
12 22.0 56 0.30 262.2 4.33 41.35 41.92
102
74.0
4
1273.
0 22.0 80 0.42 262.6
6 4.38 43.64 42.00 12
72.0 22.0 68 0.36
263.02 4.35 42.49 42.84
1271.
0 22.0 52 0.28 263.3
0 4.32 40.97 42.34 12
70.0 22.0 76 0.40
263.70 4.37 43.26 43.26
1269.
0 22.0 44 0.23 263.9
3 4.30 40.21 43.90 12
68.0 22.0 92 0.49
264.42 4.40 44.78 43.68
1267.
0 22.0 108 0.57 264.9
9 4.44 46.30 43.98 12
66.0 22.0 28 0.15
265.14 4.27 38.69 44.32
1265.
0 22.0 156 0.83 265.9
6 4.54 50.87 44.87 12
64.0 22.0 124 0.66
266.62 4.47 47.83 45.06
1263.
0 22.0 56 0.30 266.9
2 4.33 41.35 45.06 12
62.0 22.0 100 0.53
267.45 4.42 45.54 44.75
1261.
0 22.0 88 0.47 267.9
1 4.40 44.40 44.98 12
60.0 22.0 133 0.70
268.62 4.49 48.68 43.99
1259.
0 22.0 64 0.34 268.9
5 4.35 42.11 43.19 12
58.0 22.0 92 0.49
269.44 4.40 44.78 43.15
1257.
0 22.0 76 0.40 269.8
4 4.37 43.26 43.19 12
56.0 22.0 52 0.28
270.12 4.32 40.97 42.62
1255.
0 22.0 52 0.28 270.3
9 4.32 40.97 41.92 12
54.0 22.0 40 0.21
270.61 4.30 39.83 46.00
1253.
0 22.0 52 0.28 270.8
8 4.32 40.97 45.46 12
52.0 22.0 104 0.55
271.43 4.43 45.92 45.03
1251.
0 22.0 28 0.15 271.5
8 4.27 38.69 44.87 12
50.0 22.0 60 0.32
271.90 4.34 41.73 45.29
1249.
0 22.0 492 2.60 274.5
0 5.23 82.86 45.26 12
48.0 22.0 36 0.19
274.69 4.29 39.45 45.39
1247.
0 22.0 30 0.16 274.8
5 4.28 38.88 44.68 12
46.0 22.0 36 0.19
275.04 4.29 39.45 44.99
1245. 22.0 96 0.51
275.55 4.41 45.16 44.82
103
0
1244.
0 22.0 36 0.19 275.7
4 4.29 39.45 40.93 12
43.0 22.0 66 0.35
276.09 4.35 42.30 40.82
1242.
0 22.0 30 0.16 276.2
5 4.28 38.88 41.22 12
41.0 22.0 60 0.32
276.56 4.34 41.73 41.79
1240.
0 22.0 42 0.22 276.7
9 4.30 40.02 41.39 12
39.0 22.0 84 0.44
277.23 4.39 44.02 41.90
1238.
0 22.0 24 0.13 277.3
6 4.26 38.31 41.85 12
37.0 22.0 72 0.38
277.74 4.36 42.88 42.40
1236.
0 22.0 96 0.51 278.2
5 4.41 45.16 42.74 12
35.0 22.0 54 0.29
278.53 4.33 41.16 43.48
1234.
0 22.0 90 0.48 279.0
1 4.40 44.59 43.75 12
33.0 22.0 60 0.32
279.33 4.34 41.73 44.28
1232.
5 22.5 88 0.47 279.7
9 4.40 44.40 44.21 12
31.5 22.5 96 0.51
280.30 4.41 45.16 43.48
1230.
5 22.5 120 0.63 280.9
3 4.46 47.44 44.04 12
29.5 22.5 112 0.59
281.53 4.44 46.68 44.28
1228.
5 22.5 80 0.42 281.9
5 4.38 43.64 44.78 12
27.5 22.5 64 0.34
282.29 4.35 42.11 44.44
1226.
5 22.5 20 0.11 282.3
9 4.26 37.93 43.98 12
25.5 22.5 112 0.59
282.99 4.44 46.68 43.37
1224.
5 22.5 116 0.61 283.6
0 4.45 47.06 42.80 12
23.5 22.5 112 0.59
284.19 4.44 46.68 42.69
1222.
5 22.5 52 0.28 284.4
7 4.32 40.97 42.57 12
21.5 22.5 48 0.25
284.72 4.31 40.59 42.80
1220.
5 22.5 56 0.30 285.0
2 4.33 41.35 42.46 12
19.5 22.5 52 0.28
285.29 4.32 40.97 41.92
1218.
5 22.5 68 0.36 285.6
5 4.35 42.49 41.16 12
17.5 22.5 52 0.28
285.93 4.32 40.97 41.31
1216.
5 22.5 44 0.23 286.1
6 4.30 40.21 41.47
104
1215.
5 22.5 76 0.40 286.5
6 4.37 43.26 41.50 12
14.5 22.5 60 0.32
286.88 4.34 41.73 41.54
1213.
5 22.5 32 0.17 287.0
5 4.28 39.07 41.73 12
12.5 22.5 68 0.36
287.41 4.35 42.49 41.47
1211.
5 22.5 64 0.34 287.7
5 4.35 42.11 41.66 12
10.5 22.5 60 0.32
288.07 4.34 41.73 41.31
1209.
5 22.5 56 0.30 288.3
6 4.33 41.35 41.05 12
08.5 22.5 88 0.47
288.83 4.40 44.40 41.24
1207.
5 22.5 24 0.13 288.9
6 4.26 38.31 41.01 12
06.5 22.5 64 0.34
289.30 4.35 42.11 40.67
1205.
5 22.5 40 0.21 289.5
1 4.30 39.83 40.67 12
04.5 22.5 32 0.17
289.68 4.28 39.07 40.67
1203.
5 22.5 52 0.28 289.9
5 4.32 40.97 40.32 12
02.5 22.5 44 0.23
290.18 4.30 40.21 40.36
1201.
5 22.5 28 0.15 290.3
3 4.27 38.69 40.48 12
00.5 22.5 60 0.32
290.65 4.34 41.73 40.55
1199.
5 22.5 56 0.30 290.9
5 4.33 41.35 40.90 11
98.5 22.5 52 0.28
291.22 4.32 40.97 40.71
1197.
5 22.5 28 0.15 291.3
7 4.27 38.69 41.31 11
96.5 22.5 76 0.40
291.77 4.37 43.26 41.77
1195.
5 22.5 48 0.25 292.0
3 4.31 40.59 41.73 11
94.5 22.5 68 0.36
292.39 4.35 42.49 41.50
1193.
5 22.5 32 0.17 292.5
5 4.28 39.07 41.31 11
92.5 22.5 108 0.57
293.13 4.44 46.30 41.43
1191.
5 22.5 76 0.40 293.5
3 4.37 43.26 41.73 11
90.5 22.5 56 0.30
293.82 4.33 41.35 41.54
1189.
5 22.5 32 0.17 293.9
9 4.28 39.07 41.62 11
88.5 22.5 32 0.17
294.16 4.28 39.07 42.42
1187.
5 22.5 40 0.21 294.3
8 4.30 39.83 41.54
11 22.5 108 0.57 294.9 4.44 46.30 40.93
105
86.5
5
1185.
5 22.5 28 0.15 295.0
9 4.27 38.69 41.31 11
84.5 22.5 76 0.40
295.50 4.37 43.26 41.20
1183.
5 22.5 116 0.61 296.1
1 4.45 47.06 41.28 11
82.5 22.5 16 0.08
296.20 4.25 37.55 41.39
1181.
5 22.5 12 0.06 296.2
6 4.24 37.16 40.63 11
80.5 22.5 96 0.51
296.77 4.41 45.16 40.74
1179.
5 22.5 20 0.11 296.8
7 4.26 37.93 40.71 11
78.5 22.5 40 0.21
297.08 4.30 39.83 40.06
1177.
5 22.5 52 0.28 297.3
6 4.32 40.97 40.51 11
76.5 22.5 28 0.15
297.51 4.27 38.69 41.12
1175.
5 22.5 40 0.21 297.7
2 4.30 39.83 40.55 11
74.5 22.5 72 0.38
298.10 4.36 42.88 40.78
1173.
5 22.5 48 0.25 298.3
5 4.31 40.59 40.67 11
72.5 22.5 64 0.34
298.69 4.35 42.11 40.55
1171.
5 22.5 76 0.40 299.1
0 4.37 43.26 40.29 11
70.5 22.5 36 0.19
299.29 4.29 39.45 40.44
1169.
5 22.5 44 0.23 299.5
2 4.30 40.21 39.94 11
68.5 22.5 28 0.15
299.67 4.27 38.69 39.75
1167.
5 22.5 40 0.21 299.8
8 4.30 39.83 39.64 10
86.5 70.5 4.21 36.02 39.41
1085.
5 70.5 56 0.30 312.8
8 4.33 41.35 39.26 10
84.5 70.5 20 0.11
312.99 4.26 37.93 39.75
1083.
5 70.5 28 0.15 313.1
3 4.27 38.69 40.21 10
82.5 70.5 52 0.28
313.41 4.32 40.97 40.06
1081.
5 70.5 52 0.28 313.6
8 4.32 40.97 40.44 10
80.5 70.5 20 0.11
313.79 4.26 37.93 40.67
1079.
5 70.5 96 0.51 314.3
0 4.41 45.16 40.67 10
78.5 70.5 76 0.40
314.70 4.37 43.26 40.74
1077. 70.5 24 0.13
314.83 4.26 38.31 40.67
106
5
1076.
5 70.5 40 0.21 315.0
4 4.30 39.83 40.71 10
75.5 70.5 80 0.42
315.46 4.38 43.64 40.71
1074.
5 70.5 20 0.11 315.5
7 4.26 37.93 40.10 10
73.5 70.5 36 0.19
315.76 4.29 39.45 40.21
1072.
5 70.5 44 0.23 315.9
9 4.30 40.21 40.74 10
71.5 70.5 56 0.30
316.29 4.33 41.35 41.01
1070.
5 70.5 20 0.11 316.3
9 4.26 37.93 40.71 10
69.5 70.5 32 0.17
316.56 4.28 39.07 40.74
1068.
5 70.5 88 0.47 317.0
3 4.40 44.40 40.78 10
67.5 70.5 80 0.42
317.45 4.38 43.64 40.63
1066.
5 70.5 68 0.36 317.8
1 4.35 42.49 40.71 10
65.5 70.5 48 0.25
318.07 4.31 40.59 40.90
1064.
5 70.5 24 0.13 318.1
9 4.26 38.31 40.90 10
63.5 70.5 40 0.21
318.40 4.30 39.83 40.63
1062.
5 70.5 28 0.15 318.5
5 4.27 38.69 40.06 10
61.5 70.5 64 0.34
318.89 4.35 42.11 42.53
1060.
5 70.5 40 0.21 319.1
0 4.30 39.83 42.46 10
59.5 70.5 32 0.17
319.27 4.28 39.07 42.49
1058.
5 70.5 60 0.32 319.5
9 4.34 41.73 42.61 10
57.5 70.5 20 0.11
319.70 4.26 37.93 44.17
1056.
5 70.5 328 1.74 321.4
3 4.89 67.24 44.21 10
55.5 70.5 40 0.21
321.64 4.30 39.83 44.21
1054.
5 70.5 28 0.15 321.7
9 4.27 38.69 44.13 10
53.5 70.5 52 0.28
322.07 4.32 40.97 43.98
1052.
5 70.5 192 1.02 323.0
8 4.61 54.30 44.06 10
51.5 70.5 68 0.36
323.44 4.35 42.49 41.66
1050.
5 70.5 40 0.21 323.6
5 4.30 39.83 41.54 10
49.5 70.5 24 0.13
323.78 4.26 38.31 42.08
1048.
5 70.5 44 0.23 324.0
1 4.30 40.21 42.49
107
1047.
5 70.5 28 0.15 324.1
6 4.27 38.69 41.16 10
46.5 70.5 76 0.40
324.56 4.37 43.26 41.54
1045.
5 70.5 28 0.15 324.7
1 4.27 38.69 42.04 10
44.5 70.5 84 0.44
325.16 4.39 44.02 42.49
1043.
5 70.5 96 0.51 325.6
6 4.41 45.16 42.95 10
42.5 70.5 52 0.28
325.94 4.32 40.97 43.41
1041.
5 70.5 108 0.57 326.5
1 4.44 46.30 43.26 10
40.5 70.5 92 0.49
327.00 4.40 44.78 43.41
1039.
5 70.5 72 0.38 327.3
8 4.36 42.88 42.99 10
38.5 70.5 92 0.49
327.87 4.40 44.78 42.53
1037.
5 70.5 76 0.40 328.2
7 4.37 43.26 42.53 10
36.5 70.5 60 0.32
328.59 4.34 41.73 42.27
1035.
5 70.5 44 0.23 328.8
2 4.30 40.21 41.96 10
34.5 70.5 40 0.21
329.03 4.30 39.83 42.00
1033.
5 70.5 48 0.25 329.2
8 4.31 40.59 41.89 10
32.5 70.5 52 0.28
329.56 4.32 40.97 41.39
1031.
5 70.5 80 0.42 329.9
8 4.38 43.64 41.12 10
30.5 70.5 60 0.32
330.30 4.34 41.73 41.16
1029.
5 70.5 76 0.40 330.7
0 4.37 43.26 41.73 10
28.5 70.5 80 0.42
331.13 4.38 43.64 42.30
1027.
5 70.5 24 0.13 331.2
5 4.26 38.31 43.03 10
26.5 70.5 32 0.17
331.42 4.28 39.07 42.53
1025.
5 70.5 48 0.25 331.6
8 4.31 40.59 42.53 10
24.5 70.5 100 0.53
332.20 4.42 45.54 42.76
1023.
5 70.5 108 0.57 332.7
8 4.44 46.30 42.27 10
22.5 70.5 128 0.68
333.45 4.48 48.21 42.53
1021.
5 70.5 28 0.15 333.6
0 4.27 38.69 42.72 10
20.5 70.5 60 0.32
333.92 4.34 41.73 42.88
1019.
5 70.5 100 0.53 334.4
5 4.42 45.54 42.19
10 70.5 28 0.15 334.6 4.27 38.69 41.50
108
18.5
0
1017.
5 70.5 52 0.28 334.8
7 4.32 40.97 40.82 10
16.5 70.5 52 0.28
335.15 4.32 40.97 41.50
1015.
5 70.5 64 0.34 335.4
9 4.35 42.11 41.28 10
14.5 70.5 28 0.15
335.63 4.27 38.69 40.71
1013.
5 70.5 36 0.19 335.8
2 4.29 39.45 40.97 10
12.5 70.5 56 0.30
336.12 4.33 41.35 40.97
1011.
5 70.5 100 0.53 336.6
5 4.42 45.54 41.20 10
10.5 70.5 36 0.19
336.84 4.29 39.45 41.01
1009.
5 70.5 40 0.21 337.0
5 4.30 39.83 40.93 10
08.5 70.5 56 0.30
337.35 4.33 41.35 41.28
1007.
5 70.5 52 0.28 337.6
2 4.32 40.97 41.20 10
06.5 70.5 76 0.40
338.03 4.37 43.26 40.82
1005.
5 70.5 44 0.23 338.2
6 4.30 40.21 40.86 10
04.5 70.5 20 0.11
338.36 4.26 37.93 40.93
1003.
5 70.5 72 0.38 338.7
5 4.36 42.88 40.86 10
02.5 70.5 48 0.25
339.00 4.31 40.59 40.74
1001.
5 70.5 60 0.32 339.3
2 4.34 41.73 40.40 10
00.5 70.5 40 0.21
339.53 4.30 39.83 40.59
999.5 70.5 48 0.25
339.78 4.31 40.59 40.93
998.5 70.5 48 0.25
340.04 4.31 40.59 40.48
997.5 70.5 40 0.21
340.25 4.30 39.83 40.21
996.5 70.5 40 0.21
340.46 4.30 39.83 40.48
995.5 70.5 64 0.34
340.80 4.35 42.11 40.78
994.5 70.5 56 0.30
341.09 4.33 41.35 40.59
993.5 70.5 24 0.13
341.22 4.26 38.31 40.55
992.5 70.5 20 0.11
341.33 4.26 37.93 40.67
991.5 70.5 88 0.47
341.79 4.40 44.40 41.20
990.5 70.5 72 0.38
342.17 4.36 42.88 40.90
989.5 70.5 28 0.15
342.32 4.27 38.69 40.63
988.5 70.5 44 0.23
342.56 4.30 40.21 40.97
987.5 70.5 52 0.28
342.83 4.32 40.97 41.20
986.5 70.5 96 0.51
343.34 4.41 45.16 41.28
985.5 70.5 32 0.17
343.51 4.28 39.07 40.78
984.5 70.5 28 0.15
343.66 4.27 38.69 40.78
109
983.5 70.5 60 0.32
343.97 4.34 41.73 41.62
982.5 70.5 44 0.23
344.21 4.30 40.21 41.35
981.5 70.5 96 0.51
344.71 4.41 45.16 41.43
980.5 70.5 20 0.11
344.82 4.26 37.93 42.76
979.5 70.5 28 0.15
344.97 4.27 38.69 42.99
978.5 70.5 132 0.70
345.67 4.49 48.59 42.69
977.5 70.5 24 0.13
345.79 4.26 38.31 42.53
976.5 70.5 104 0.55
346.34 4.43 45.92 41.96
975.5 70.5 172 0.91
347.25 4.57 52.39 41.92
974.5 70.5 52 0.28
347.53 4.32 40.97 42.00
973.5 70.5 28 0.15
347.68 4.27 38.69 41.35
972.5 70.5 28 0.15
347.83 4.27 38.69 41.85
971.5 70.5 36 0.19
348.02 4.29 39.45 41.62
970.5 70.5 16 0.08
348.10 4.25 37.55 40.71
969.5 70.5 36 0.19
348.29 4.29 39.45 41.16
968.5 70.5 64 0.34
348.63 4.35 42.11 42.08
967.5 70.5 76 0.40
349.03 4.37 43.26 43.03
966.5 70.5 80 0.42
349.46 4.38 43.64 43.29
965.5 70.5 76 0.40
349.86 4.37 43.26 43.83
964.5 70.5 100 0.53
350.39 4.42 45.54 44.13
963.5 70.5 124 0.66
351.04 4.47 47.83 43.87
962.5 70.5 128 0.68
351.72 4.48 48.21 44.09
961.5 70.5 64 0.34
352.06 4.35 42.11 43.71
960.5 70.5 72 0.38
352.44 4.36 42.88 43.14
959.5 70.5 68 0.36
352.80 4.35 42.49 42.49
958.5 70.5 36 0.19
352.99 4.29 39.45 41.66
957.5 70.5 100 0.53
353.52 4.42 45.54 41.24
956.5 70.5 40 0.21
353.73 4.30 39.83 40.90
955.5 70.5 16 0.08
353.82 4.25 37.55 40.48
954.5 70.5 32 0.17
353.98 4.28 39.07 39.98
953.5 70.5 36 0.19
354.18 4.29 39.45 40.29
952.5 70.5 84 0.44
354.62 4.39 44.02 39.83
951.5 70.5 28 0.15
354.77 4.27 38.69 40.06
950.5 70.5 28 0.15
354.92 4.27 38.69 40.21
949.5 70.5 16 0.08
355.00 4.25 37.55 40.40
948.5 70.5 68 0.36
355.36 4.35 42.49 40.36
947.5 70.5 52 0.28
355.64 4.32 40.97 39.94
946.5 70.5 64 0.34
355.97 4.35 42.11 39.98
945.5 70.5 32 0.17
356.14 4.28 39.07 40.44
944.5 70.5 52 0.28
356.42 4.32 40.97 40.55
943.5 70.5 32 0.17
356.59 4.28 39.07 40.25
942.5 70.5 40 0.21
356.80 4.30 39.83 40.10
941.5 70.5 32 0.17
356.97 4.28 39.07 40.17
940.5 70.5 76 0.40
357.37 4.37 43.26 40.13
110
939.5 70.5 28 0.15
357.52 4.27 38.69 40.32
938.5 70.5 36 0.19
357.71 4.29 39.45 40.32
937.5 70.5 36 0.19
357.90 4.29 39.45 40.60
936.5 70.5 72 0.38
358.28 4.36 42.88 40.68
935.5 70.5 28 0.15
358.43 4.27 38.69 40.18
934.5 70.5 72 0.38
358.81 4.36 42.88 40.80
933.5 70.5 32 0.17
358.98 4.28 39.07 40.72
932.5 70.5 69 0.37
359.35 4.36 42.59 40.69
931.5 70.5 40 0.21
359.56 4.30 39.83 40.42
930.5 70.5 24 0.13
359.68 4.26 38.31 40.34
929.5 70.5 93 0.49
360.18 4.41 44.87 39.92
928.5 70.5 28 0.15
360.32 4.27 38.69 40.31
927.5 70.5 32 0.17
360.49 4.28 39.07 39.99
926.5 70.5 44 0.23
360.73 4.30 40.21 40.30
925.5 70.5 20 0.11
360.83 4.26 37.93 40.91
924.5 71.0 28 0.15
360.98 4.27 38.69 40.51
923.5 71.0 72 0.38
361.36 4.36 42.88 40.74
922.5 71.0 36 0.19
361.55 4.29 39.45 40.59
921.5 71.0 72 0.38
361.93 4.36 42.88 40.59
920.5 71.0 88 0.47
362.40 4.40 44.40 40.86
919.5 71.0 52 0.28
362.67 4.32 40.97 40.97
918.5 71.0 52 0.28
362.95 4.32 40.97 40.71
917.5 71.0 16 0.08
363.03 4.25 37.55 40.78
916.5 71.0 44 0.23
363.27 4.30 40.21 41.09
915.5 71.0 48 0.25
363.52 4.31 40.59 40.51
914.5 71.0 40 0.21
363.73 4.30 39.83 41.09
913.5 71.0 44 0.23
363.96 4.30 40.21 41.35
912.5 71.0 44 0.23
364.20 4.30 40.21 41.58
911.5 71.0 104 0.55
364.75 4.43 45.92 41.47
910.5 71.0 28 0.15
364.90 4.27 38.69 41.47
909.5 71.0 112 0.59
365.49 4.44 46.68 41.35
908.5 71.0 80 0.42
365.91 4.38 43.64 41.50
907.5 71.0 40 0.21
366.12 4.30 39.83 41.28
906.5 71.0 32 0.17
366.29 4.28 39.07 40.59
905.5 71.0 48 0.25
366.55 4.31 40.59 40.86
904.5 71.0 28 0.15
366.70 4.27 38.69 40.13
903.5 71.0 60 0.32
367.01 4.34 41.73 39.98
902.5 71.0 20 0.11
367.12 4.26 37.93 40.32
901.5 71.0 32 0.17
367.29 4.28 39.07 40.29
900.5 71.0 56 0.30
367.58 4.33 41.35 40.13
899.5 71.0 36 0.19
367.77 4.29 39.45 40.48
898.5 71.0 64 0.34
368.11 4.35 42.11 40.36
897.5 71.0 76 0.40
368.52 4.37 43.26 40.67
896.5 71.0 28 0.15
368.66 4.27 38.69 40.82
111
895.5 71.0 32 0.17
368.83 4.28 39.07 40.63
894.5 71.0 64 0.34
369.17 4.35 42.11 40.71
893.5 71.0 48 0.25
369.43 4.31 40.59 40.59
892.5 71.0 52 0.28
369.70 4.32 40.97 40.13
891.5 71.0 48 0.25
369.95 4.31 40.59 40.55
890.5 71.0 36 0.19
370.15 4.29 39.45 40.51
889.5 71.0 44 0.23
370.38 4.30 40.21 40.36
888.5 71.0 52 0.28
370.65 4.32 40.97 40.40
887.5 71.0 28 0.15
370.80 4.27 38.69 40.51
886.5 71.0 72 0.38
371.18 4.36 42.88 40.32
885.5 71.0 28 0.15
371.33 4.27 38.69 40.48
884.5 71.0 48 0.25
371.58 4.31 40.59 40.67
883.5 71.0 52 0.28
371.86 4.32 40.97 41.01
882.5 71.0 64 0.34
372.20 4.35 42.11 41.05
881.5 71.0 28 0.15
372.35 4.27 38.69 40.67
880.5 71.0 52 0.28
372.62 4.32 40.97 40.71
879.5 71.0 64 0.34
372.96 4.35 42.11 40.55
878.5 71.0 88 0.47
373.43 4.40 44.40 40.74
877.5 71.0 32 0.17
373.60 4.28 39.07 40.67
876.5 71.0 32 0.17
373.76 4.28 39.07 41.12
875.5 71.0 32 0.17
373.93 4.28 39.07 40.93
874.5 71.0 32 0.17
374.10 4.28 39.07 40.71
873.5 71.0 72 0.38
374.48 4.36 42.88 40.90
872.5 71.0 56 0.30
374.78 4.33 41.35 41.28
871.5 71.0 76 0.40
375.18 4.37 43.26 41.12
870.5 71.0 32 0.17
375.35 4.28 39.07 41.20
869.5 71.0 40 0.21
375.56 4.30 39.83 41.58
868.5 71.0 108 0.57
376.14 4.44 46.30 41.05
867.5 71.0 72 0.38
376.52 4.36 42.88 41.31
866.5 71.0 16 0.08
376.60 4.25 37.55 40.82
865.5 71.0 40 0.21
376.81 4.30 39.83 40.78
864.5 71.0 72 0.38
377.19 4.36 42.88 40.74
863.5 71.0 16 0.08
377.28 4.25 37.55 40.32
862.5 71.0 84 0.44
377.72 4.39 44.02 39.94
861.5 71.0 24 0.13
377.85 4.26 38.31 40.32
860.5 71.0 28 0.15
378.00 4.27 38.69 41.12
859.5 71.0 36 0.19
378.19 4.29 39.45 41.70
858.5 71.0 64 0.34
378.53 4.35 42.11 41.92
857.5 71.0 32 0.17
378.70 4.28 39.07 42.84
856.5 71.0 56 0.30
378.99 4.33 41.35 42.78
855.5 71.0 124 0.66
379.65 4.47 47.83 43.16
854.5 71.0 132 0.70
380.35 4.49 48.59 44.00
853.5 71.0 40 0.21
380.56 4.30 39.83 44.11
852.5 71.0 180 0.95
381.51 4.58 53.16 44.19
112
851.5 71.0 18 0.10
381.61 4.25 37.74 44.15
850.5 71.0 68 0.36
381.97 4.35 42.49 43.62
849.5 71.0 124 0.66
382.62 4.47 47.83 43.20
848.5 71.0 76 0.40
383.02 4.37 43.26 43.16
847.5 71.0 40 0.21
383.24 4.30 39.83 41.71
846.5 71.0 52 0.28
383.51 4.32 40.97 42.23
845.5 71.0 68 0.36
383.87 4.35 42.49 41.85
844.5 71.0 88 0.47
384.34 4.40 44.40 41.24
843.5 71.0 36 0.19
384.53 4.29 39.45 41.35
842.5 71.0 28 0.15
384.68 4.27 38.69 41.28
841.5 71.0 72 0.38
385.06 4.36 42.88 41.54
840.5 71.0 28 0.15
385.21 4.27 38.69 41.16
839.5 71.0 60 0.32
385.52 4.34 41.73 41.50
838.5 71.0 88 0.47
385.99 4.40 44.40 41.47
837.5 71.0 32 0.17
386.16 4.28 39.07 41.50
836.5 71.0 80 0.42
386.58 4.38 43.64 41.47
835.5 71.0 28 0.15
386.73 4.27 38.69 42.11
834.5 71.0 124 0.66
387.39 4.47 47.83 42.61
833.5 71.0 32 0.17
387.55 4.28 39.07 42.04
832.5 71.0 32 0.17
387.72 4.28 39.07 42.30
831.5 71.0 68 0.36
388.08 4.35 42.49 42.49
830.5 71.0 96 0.51
388.59 4.41 45.16 43.03
829.5 71.0 112 0.59
389.18 4.44 46.68 42.53
828.5 71.0 28 0.15
389.33 4.27 38.69 42.53
827.5 71.0 60 0.32
389.65 4.34 41.73 42.91
826.5 71.0 100 0.53
390.18 4.42 45.54 42.53
825.5 71.0 84 0.44
390.62 4.39 44.02 41.85
824.5 71.0 72 0.38
391.00 4.36 42.88 41.01
823.5 71.0 32 0.17
391.17 4.28 39.07 41.12
822.5 71.0 72 0.38
391.55 4.36 42.88 40.93
821.5 71.0 28 0.15
391.70 4.27 38.69 40.90
820.5 71.0 24 0.13
391.83 4.26 38.31 40.44
819.5 71.0 24 0.13
391.96 4.26 38.31 40.48
818.5 71.0 40 0.21
392.17 4.30 39.83 40.67
817.5 71.0 40 0.21
392.38 4.30 39.83 40.59
816.5 71.0 96 0.51
392.89 4.41 45.16 40.67
815.5 71.0 36 0.19
393.08 4.29 39.45 40.90
814.5 71.0 76 0.40
393.48 4.37 43.26 41.39
813.5 71.0 52 0.28
393.76 4.32 40.97 41.39
812.5 71.0 64 0.34
394.09 4.35 42.11 41.54
811.5 71.0 36 0.19
394.29 4.29 39.45 40.97
810.5 71.0 48 0.25
394.54 4.31 40.59 40.78
809.5 71.0 76 0.40
394.94 4.37 43.26 40.55
808.5 71.0 40 0.21
395.15 4.30 39.83 40.71
113
807.5 71.0 56 0.30
395.45 4.33 41.35 40.40
806.5 71.0 36 0.19
395.64 4.29 39.45 40.40
805.5 71.0 16 0.08
395.72 4.25 37.55 40.25
804.5 71.0 52 0.28
396.00 4.32 40.97 40.10
803.5 71.0 68 0.36
396.36 4.35 42.49 40.82
802.5 71.0 32 0.17
396.53 4.28 39.07 41.43
801.5 71.0 36 0.19
396.72 4.29 39.45
800.5 71.0 32 0.17
396.89 4.28 39.07
799.5 71.0 60 0.32
397.21 4.34 41.73
798.5 71.0 116 0.61
397.82 4.45 47.06
797.5 71.0 120 0.63
398.46 4.46 47.44
Plutonium Dating from Michael Ketterer, Northern Arizona University
Depth (cm) Bq/kg Bg/kg SD 240/239 240239 sd
0.25 0.23 0.02 0.196 0.011 0.75 0.24 0.01 0.184 0.019 1.25 0.29 0.02 0.229 0.024 1.75 0.44 0.02 0.179 0.016 2.25 1.06 0.03 0.179 0.007 2.75 3.87 0.04 0.186 0.005 3.25 13.80 0.09 0.180 0.003 3.75 4.26 0.04 0.185 0.005 4.25 0.06 0.01 4.75 0.00 5.25 0.00 5.75 0.00 6.25 0.00 6.75 0.00 7.25 0.00