# Eclipse Icefield 2002 Cores 1,000 Year Major Ions and Isotope Data #----------------------------------------------------------------------- # World Data Service for Paleoclimatology, Boulder # and # NOAA Paleoclimatology Program # National Centers for Environmental Information (NCEI) #----------------------------------------------------------------------- # Template Version 3.0 # Encoding: UTF-8 # NOTE: Please cite Publication, and Online_Resource and date accessed when using these data. # If there is no publication information, please cite Investigators, Title, and Online_Resource and date accessed. # # Online_Resource: https://www.ncdc.noaa.gov/paleo/study/30877 # Description: NOAA Landing Page # Online_Resource: https://www.ncei.noaa.gov/pub/data/paleo/icecore/trop/eclipse/eclipse2002core3ion-iso.txt # Description: NOAA location of the template # # Original_Source_URL: # Description: # # Description/Documentation lines begin with # # Data lines have no # # # Data Type: Ice Cores # # Dataset DOI: # # Parameter_Keywords: chemistry, oxygen isotopes, hydrogen isotopes #--------------------------------------- # Contribution_Date # Date: 2020-07-29 #--------------------------------------- # File_Last_Modified_Date # Date: 2020-07-29 #--------------------------------------- # Title # Study_Name: Eclipse Icefield 2002 Cores 1,000 Year Major Ions and Isotope Data #--------------------------------------- # Investigators # Investigators: Yalcin, K.; Wake, C.; Kreutz, K. #--------------------------------------- # Description_Notes_and_Keywords # Description: Major ions (Na, NH4, K, Mg, Ca, Cl, NO3, SO4, C2O4) and isotope (d18O, dD) data from Eclise 2002 ice cores 2 and 3. # Provided Keywords: ice cores, stable isotopes, major ions, accumulation, time series #--------------------------------------- # Publication # Authors: Yalcin, K., C.P. Wake, K.J. Kreutz, M.S. Germani, and S.I. Whitlow # Published_Date_or_Year: 2007 # Published_Title: Ice core paleovolcanic records from the St. Elias Mountains, Yukon, Canada # Journal_Name: Journal of Geophysical Research # Volume: 112 # Edition: # Issue: # Pages: D08102 # Report_Number: # DOI: 10.1029/2006JD007497 # Online_Resource: # Full_Citation: # Abstract: We previously reported a record of regionally significant volcanic eruptions in the North Pacific using an ice core from Eclipse Icefield (St. Elias Mountains, Yukon, Canada). The acquisition of two new ice cores from Eclipse Icefield, along with the previously available Eclipse Icefield and Mount Logan Northwest Col ice cores, allows us to extend our record of North Pacific volcanism to 550 years before present using a suite of four ice cores spanning an elevation range of 3–5 km. Comparison of volcanic sulfate flux records demonstrates that the results are highly reproducible, especially for the largest eruptions such as Katmai (A.D. 1912). Correlation of volcanic sulfate signals with historically documented eruptions indicates that at least one-third of the eruptions recorded in St. Elias ice cores are from Alaskan and Kamchatkan volcanoes. Although there are several moderately large (volcanic explosivity index (VEI) = 4) eruptions recorded in only one core from Eclipse Icefield, the use of multiple cores provides signals in at least one core from all known VEI = 4 eruptions in Alaska and Kamchatka since A.D. 1829. Tephrochronological evidence from the Eclipse ice cores documents eruptions in Alaska (Westdahl, Redoubt, Trident, and Katmai), Kamchatka (Avachinsky, Kliuchevoskoi, and Ksudach), and Iceland (Hekla). Several unidentified tephra-bearing horizons, with available geochemical evidence suggesting Alaskan and Kamchatkan sources, were also found. We present a reconstruction of annual volcanic sulfate loading for the North Pacific troposphere based on our ice core data, and we provide a detailed assessment of the atmospheric and climatic effects of the Katmai eruption. #--------------------------------------- # Publication # Authors: Yalcin, K., C.P. Wake, K.J. Kreutz, M.S. Germani, and S.I. Whitlow # Published_Date_or_Year: 2006 # Published_Title: Ice core evidence for a second volcanic eruption around 1809 in the Northern Hemisphere # Journal_Name: Geophysical Research Letters # Volume: 33 # Edition: # Issue: # Pages: L14706 # Report_Number: # DOI: 10.1029/2006GL026013 # Online_Resource: # Full_Citation: # Abstract: A volcanic signal observed in ice cores from both polar regions six years prior to Tambora is attributed to an unknown tropical eruption in 1809. Recovery of dacitic tephra from the 1809 horizon in a Yukon ice core (Eclipse) that is chemically distinct from andesitic 1809 tephra found in Antarctic ice cores indicates a second eruption in the Northern Hemisphere at this time. Together with the similar magnitude and timing of the 1809 volcanic signal in the Arctic and Antarctic, this could suggest a large tropical eruption produced the sulfate and Antarctic tephra and a minor Northern Hemisphere eruption produced the Eclipse tephra. Nonetheless, the possibility that there were coincidental eruptions of similar magnitude in both hemispheres, rather than a single tropical eruption, should not be discounted. Correctly attributing the source of the 1809 volcanic signal has important implications for modeling the magnitude and latitudinal distribution of volcanic radiative forcing. #--------------------------------------- # Publication # Authors: Yalcin, K., C.P. Wake, S. Kang, K.J. Kreutz, and S.I. Whitlow # Published_Date_or_Year: 2006 # Published_Title: Seasonal and spatial variability in snow chemistry at Eclipse Icefield, Yukon, Canada # Journal_Name: Annals of Glaciology # Volume: 43 # Edition: # Issue: # Pages: 230-238 # Report_Number: # DOI: 10.3189/172756406781811998 # Online_Resource: # Full_Citation: # Abstract: Samples collected from four snow pits at Eclipse Icefield, Yukon, Canada, were analyzed for stable isotopes and major ions to assess seasonal and spatial variability in snow chemistry. Accumulation since the end of the 2001 summer season over the 0.1 km2 area sampled ranges from 0.77 to 1.16mw.e. Snow-pit stratigraphy and chemical records demonstrate that the low accumulation at pit 3 is due to an under-representation of winter snow accumulation at that site. For all major-ion species, chemical concentrations are independent of snow accumulation rate. Seasonal variations are evident in the major-ion records and can be divided between sea-salt species (Na+, Cl-) that peak in late fall to winter, and dust (Ca2+, Mg2+, K+) and other species (NH4 +, NO3 -, SO4 2–, C2O2 2–) that peak in late spring to summer. The signal common to all four snow pits identified by empirical orthogonal function analysis ranges from 49% of the total variance for Na+ and Cl- to as high as 80% of the total variance for SO4 2–. There is greater spatial variability in species associated with coarse-mode particles (Na+, Cl-, Ca2+, Mg2+) than in species present mainly in accumulation-mode aerosols (SO4 2–, NH4 +) or in the gas phase (NO3 -). #--------------------------------------- # Publication # Authors: Yalcin, K., C.P. Wake, S. Whitlow, and K. Kreutz # Published_Date_or_Year: 2006 # Published_Title: A 1000-year record of forest fire activity from Eclipse Icefield, Yukon, Canada # Journal_Name: The Holocene # Volume: 16 # Edition: # Issue: # Pages: 200-209 # Report_Number: # DOI: 10.1191/0959683606hl920rp # Online_Resource: # Full_Citation: # Abstract: A 1000-yr record of forest fire activity has been developed using three annually dated ice cores from Eclipse Icefield, Yukon, Canada. Forest fire signals were identified as NH4+ residuals above a robust spline and corroborated by an empirical orthhogonal function (EOF) analysis that identified a chemical association in the NH4+, C2O42- and K+ records similar to that observed in forest fire plumes. These statistical techniques yielded similar records of forest fire activity, although the EOF analysis provides more conservative identification of forest fire signals. Comparison of forest fire signals in the Eclipse ice cores with the record of annual area burned in Alaska and the Yukon demonstrates that 80% of high fire years in Alaska and 79% of high fire years in the Yukon are identifiable as NH4+ concentration residuals in at least one core from Eclipse Icefield, although any individual core records 36–67% of these events. The Eclipse ice cores record high fire activity in the AD 1760s, 1780s, 1840s, 1860s, 1880s, 1890s, 1920s–1940s and 1980s. Peak fire activity occurred in the 1890s, possibly reflecting anthropogenic ignition sources associated with the large influx of people to the Yukon during the Klondike Gold Rush. Periods of low fire activity are evident during the 1770s, 1810s–1830s, 1850s, 1950s and 1960s. Extending our proxy of fire activity to AD 1000 using annual NH4+ concentrations from our one core that extends back this far provides evidence of high fire activity from 1240 to 1410 during the waning stages of the 'Mediaeval Warm Period'. #--------------------------------------- # Publication # Authors: Fisher, D.A., J. Bourgeois, M. Demuth, R. Koerner, M. Parnandi, J. Sekerka, C. Zdanowicz, J. Zheng, C. Wake, K. Yalcin, P. Mayewski, K. Kreutz, E. Osterberg, D. Dahl-Jensen, K. Goto-Azuma, G. Holdsworth, E. Steig, S. Rupper, and M. Wasckiewicz # Published_Date_or_Year: 2004 # Published_Title: Stable isotope records from Mount Logan and Eclipse ice cores and nearby Jellybean Lake; water cycle of the North Pacific over 2000 years and over 5 vertical kilometers; sudden shifts and tropical connections # Journal_Name: Geographie Physique et Quaternaire # Volume: 58 # Edition: # Issue: 2-3 # Pages: 9033-9048 # Report_Number: # DOI: 10.7202/013147ar # Online_Resource: # Full_Citation: # Abstract: Three ice cores recovered on or near Mount Logan, together with a nearby lake record (Jellybean Lake), cover variously 500 to 30 000 years. This suite of records offers a unique view of the lapse rate in stable isotopes from the lower to upper troposphere. The region is climatologically important, being beside the Cordilleran pinning-point of the Rossby Wave system and the Aleutian Low. Comparison of stable isotope series over the last 2000 years and model simulations suggest sudden and persistent shifts between modern (mixed) and zonal flow regimes of water vapour transport to the Pacific Northwest. The last such shift was in A.D. 1840. Model simulations for modern and "pure" zonal flow suggest that these shifts are consistent regime changes between these flow types, with predominantly zonal flow prior to ca. A.D. 1840 and modern thereafter. The 5.4 and 0.8 km asl records show a shift at A.D. 1840 and another at A.D. 800. It is speculated that the A.D. 1840 regime shift coincided with the end of the Little Ice Age and the A.D. 800 shift with the beginning of the European Medieval Warm Period. The shifts are very abrupt, taking only a few years at most. #--------------------------------------- # Publication # Authors: Fisher, D., E. Osterberg, A. Dyke, D. Dahl Jensen, M. Demuth, C. Zdanowicz, J. Bourgeois, R. M. Koerner, P. Mayewski, C. Wake, K. Kreutz, E. Steig, J. Zheng, K. Yalcin, K. Goto-Azuma, B. Luckman, and S. Rupper, # Published_Date_or_Year: 2008 # Published_Title: The Mt. Logan Holocene Late-Wisconsin isotope record: tropical Pacific-Yukon connection # Journal_Name: The Holocene # Volume: 18 # Edition: # Issue: # Pages: 667-677 # Report_Number: # DOI: 10.1177/0959683608092236 # Online_Resource: # Full_Citation: # Abstract: The ice core recovered from Prospector Russell Col on Mt Logan (5.4 km a.s.l.), in the Yukon spans over 20 000 years. This unique record offers a Pacific view of the stable isotope and chemical record from the Lateglacial to the present. The timescale is based on seasonal counted years, the largest known volcanic acid signatures and the major shift in stable isotopes and chemistry at the end of the Younger Dryas. There are large and sustained changes in the stable isotopic record that are anti-correlated with marine and continental chemistry series. The oxygen-18 in this area is not a proxy for palaeotemperature but rather for source region. The last major isotope shift in AD 1840 in d(18O) and chemistry is compared with the Quinn's ENSO record. During periods of more frequent La Niña (stronger tropical easterlies) there is more zonal flow of water vapour transport to the Pacific Northwest, d(18O) values are larger and the deuterium excess d smaller. These periods coincide with periods of lower accumulation/precipitation in southern Yukon. The Holocene d(18O) record indicates many large shifts between the meridional (strong El Niño) and zonal (La Niña). Comparison of the Logan isotopic record and the moisture/temperature-sensitive time series of peat bog inception dates for the Northwest shows a strong correlation (0.36) that points to high accumulation rates coincident with low d(18O) and enhanced meridional flow. Major changes in the core at 4200 BP and 7000-8000 BP point to enhanced meridional flow, which coincide with big changes in the Pacific palaeorecords of the balance between El Niño and La Niña. 4200 BP seems to have inaugurated the 'modern' ENSO world. #--------------------------------------- # Publication # Authors: Kelsey, E.P., C.P. Wake, K. Yalcin, and K. Kreutz # Published_Date_or_Year: 2012 # Published_Title: Eclipse ice core accumulation and stable isotope variability as an indicator of North Pacific climate # Journal_Name: Journal of Climate # Volume: 25 # Edition: # Issue: # Pages: 6426-6440 # Report_Number: # DOI: 10.1175/JCLI-D-11-00389.1. # Online_Resource: # Full_Citation: # Abstract: The high accumulation rate and negligible amount of melt at Eclipse Icefield (3017 m) in the Saint Elias Range of Yukon, Canada, allows for the preservation of a high-resolution isotopic and glaciochemical records valuable for reconstruction of climatic variables. Each of the three Eclipse ice cores have a well-constrained depth-age scale with dozens of reference horizons over the twentieth century that permits an exceptional level of confidence in the results of the current calibration exercise. Stacked time series of accumulation and stable isotopes were divided into cold and warm seasons and seasons of extreme high and extreme low accumulation and stable isotope values (eight groups). For each group, season-averaged composites of 500-hPa geopotential height grids, and the individual seasons that constitute them, were analyzed to elucidate common anomalous flow patterns. This analysis shows that the most fractionated isotopes and lowest accumulation cold seasons reflect a more zonal height pattern in the North Pacific associated with negative Pacific-North American (PNA) and Pacific decadal oscillation (PDO) indices. Conversely, the least fractionated isotopes and highest accumulation cold seasons are associated with a positive PNA pattern. Although only a maximum of approximately 20% of the total number of accumulation and stable isotope seasons exhibit a relatively consistent relationship with 500-hPa geopotential height patterns, these results support the hypothesis that the most extreme accumulation and extreme isotope cold-season values in the Saint Elias Mountains are related to consistent atmospheric circulation and oceanic sea surface temperature patterns. #--------------------------------------- # Publication # Authors: Zdanowicz, C.M., D. Fisher, J. Bourgeois, M. Demuth, J. Zheng, P. Mayewski, K. Kreutz, E. Osterberg, K. Yalcin, C. Wake, E.J. Steig, D. Froese, and K. Goto_Azuma # Published_Date_or_Year: 2014 # Published_Title: Ice cores from the St. Elias Mountains, Yukon Territory, Canada: their significance for climate, atmospheric composition, and volcanism in the North Pacific region # Journal_Name: Arctic # Volume: 67 # Edition: # Issue: # Pages: 35-57 # Report_Number: # DOI: 10.14430/arctic4352 # Online_Resource: # Full_Citation: # Abstract: A major achievement in research supported by the Kluane Lake Research Station was the recovery, in 2001 - 02, of a suite of cores from the icefields of the central St. Elias Mountains, Yukon, by teams of researchers from Canada, the United States, and Japan. This project led to the development of parallel, long (103-104 year) ice-core records of climate and atmospheric change over an altitudinal range of more than 2 km, from the Eclipse Icefield (3017 m) to the ice-covered plateau of Mt. Logan (5340 m). These efforts built on earlier work recovering single ice cores in this region. Comparison of these records has allowed for variations in climate and atmospheric composition to be linked with changes in the vertical structure and dynamics of the North Pacific atmosphere, providing a unique perspective on these changes over the Holocene. Owing to their privileged location, cores from the St. Elias Icefields also contain a remarkably detailed record of aerosols from various sources around or across the North Pacific. In this paper we review major scientific findings from the study of St. Elias Mountain ice cores, focusing on five main themes: (1) The record of stable water isotopes (d18O, dD), which has unique characteristics that differ from those of Greenland, other Arctic ice cores, and even among sites in the St. Elias; (2) the snow accumulation history; (3) the record of pollen, biomass burning aerosol, and desert dust deposition; (4) the record of long-range air pollutant deposition (sulphate and lead); and (5) the record of paleo-volcanism. Our discussion draws on studies published since 2000, but based on older ice cores from the St. Elias Mountains obtained in 1980 and 1996. #--------------------------------------- # Publication # Authors: Gross, B.H., K. Kreutz, E. Osterberg, J. McConnell, M. Handley, C. Wake, and K. Yalcin # Published_Date_or_Year: 2012 # Published_Title: Constraining recent lead pollution sources in the North Pacific using ice core stable lead isotopes # Journal_Name: Journal of Geophysical Research # Volume: 117 # Edition: # Issue: # Pages: D16307 # Report_Number: # DOI: 10.1029/2011JD017270 # Online_Resource: # Full_Citation: # Abstract: Trends and sources of lead (Pb) aerosol pollution in the North Pacific rim of North America from 1850 to 2001 are investigated using a high-resolution (subannual to annual) ice core record recovered from Eclipse Icefield (3017 masl; St. Elias Mountains, Canada). Beginning in the early 1940s, increasing Pb concentration at Eclipse Icefield occurs coevally with anthropogenic Pb deposition in central Greenland, suggesting that North American Pb pollution may have been in part or wholly responsible in both regions. Isotopic ratios (208Pb/207Pb and 206Pb/207Pb) from 1970 to 2001 confirm that a portion of the Pb deposited at Eclipse Icefield is anthropogenic, and that it represents a variable mixture of East Asian (Chinese and Japanese) emissions transported eastward across the Pacific Ocean and a North American component resulting from transient meridional atmospheric flow. Based on comparison with source material Pb isotope ratios, Chinese and North American coal combustion have likely been the primary sources of Eclipse Icefield Pb over the 1970–2001 time period. The Eclipse Icefield Pb isotope composition also implies that the North Pacific mid-troposphere is not directly impacted by transpolar atmospheric flow from Europe. Annually averaged Pb concentrations in the Eclipse Icefield ice core record show no long-term trend during 1970–2001; however, increasing208Pb/207Pb and decreasing 206Pb/207Pb ratios reflect the progressive East Asian industrialization and increase in Asian pollutant outflow. The post-1970 decrease in North American Pb emissions is likely necessary to explain the Eclipse Icefield Pb concentration time series. When compared with low (lichen) and high (Mt. Logan ice core) elevation Pb data, the Eclipse ice core record suggests a gradual increase in pollutant deposition and stronger trans-Pacific Asian contribution with rising elevation in the mountains of the North Pacific rim. #--------------------------------------- # Publication # Authors: Kochtitzky, W., D. A. Winski, E. McConnell, K. J. Kreutz, S. Campbell, E. Enderlin, L. Copland, S. Williamson, B. Main, and H. Jiskoot # Published_Date_or_Year: 2020 # Published_Title: Climate and surging of Donjek Glacier, Yukon, Canada # Journal_Name: Arctic, Antarctic, and Alpine Research, # Volume: # Edition: # Issue: # Pages: # Report_Number: # DOI: 10.1080/15230430.2020.1744397 # Online_Resource: # Full_Citation: # Abstract: Links between climate and glacier surges are poorly understood but are required to enable prediction of surges and mitigation of associated hazards. Here, we investigate the role of snow accumulation, rain, and temperature on surge periodicity, area changes, and timing of surge initiation since the 1930s at Donjek Glacier, Yukon, Canada. Snow accumulation measured in three ice cores collected at Eclipse Icefield indicates that a cumulative accumulation of 15.5 ± 1.46 or 16.6 ± 2.0 m w.e. occurred in the ten to twelve years between each of its last eight surges, depending on ice motion spatiotemporal offset corrections. Although we find consistent snow accumulation between surges, the transient snow line has risen 10.3 m decade-1 vertically since the 1950s, and Burwash Landing weather station records indicate a 0.5°C decade-1 increase in mean annual air temperature since the 1960s. Changes in surface mass balance are accompanied by a consistent surge interval but decreasing surge extent. The three recent surge events initiated in years with the rainiest summers on record. These findings highlight a complex interplay between external (i.e., climate) and internal glacier processes that control surging at Donjek Glacier, with climate having a more direct influence on surge extent than on recurrence interval. #--------------------------------------- # Funding_Agency # Funding_Agency_Name: US National Science Foundation # Grant: #--------------------------------------- # Site_Information # Site_Name: Eclipse Icefield # Location: North America>Canada>Yukon Territory # Northernmost_Latitude: 60.51 # Southernmost_Latitude: 60.51 # Easternmost_Longitude: -139.47 # Westernmost_Longitude: -139.47 # Elevation: 3017 #--------------------------------------- # Data_Collection # Collection_Name: Eclipse2002Core3ion-iso # First_Year: 1909 # Last_Year: 2002 # Time_Unit: Year CE # Core_Length: 106 m # Notes: #--------------------------------------- # Chronology_Information # Chronology: #--------------------------------------- # Variables # Data variables follow that are preceded by "##" in columns one and two. # Variables list, one per line, shortname-tab-longname components (9 components: what, material, error, units, seasonality, archive, detail, method, C or N for Character or Numeric data) ## top_z depth at sample end,,,meter,,ice cores,corrected,,N,meter water equivalent; density corrected ## bot_z depth at sample start,,,meter,,ice cores,corrected,,N,meter water equivalent; density corrected ## layer_we sample thickness,,,centimeter,,ice cores,corrected,,N,centimeter water equivalent; density corrected ## year ice age,,,year Common Era,,ice cores,,,N,see publications for details on timescale construction ## d18O delta 18O,bulk ice,,per mil SMOW,,ice cores,,isotope ratio mass spectrometry,N, ## d2H delta 2H,bulk ice,,per mil SMOW,,ice cores,,isotope ratio mass spectrometry,N, ## Na sodium,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,sodium ion ## NH4 ammonium,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,ammonium ion ## K potassium,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,potassium ion ## Mg magnesium,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,magnesium ion ## Ca calcium,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,calcium ion ## Cl chloride,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,chloride ion ## NO3 nitrate,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,nitrate ion ## SO4 sulfate,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,sulfate ion ## C2O4 oxalate,bulk ice,,microequivalent per liter,,ice cores,,ion chromatography,N,oxalate ion #------------------------ # Data: # Data lines follow (have no #) # Data line format - tab-delimited text, variable short name as header # Missing_Values: # top_z bot_z layer_we year d180 dD Na NH4 K Mg Ca Cl NO3 SO4 C2O4 0.00 0.01 0.95 2002.50 -27.58 NaN 0.06 1.42 0.07 0.47 2.01 0.22 1.11 1.86 0.27 0.01 0.02 0.95 2002.48 -26.08 NaN 0.17 2.38 0.18 1.62 9.55 0.38 1.77 3.66 1.02 0.02 0.03 0.95 2002.47 -27.77 NaN 0.07 0.97 0.05 0.28 1.51 0.42 1.86 1.27 0.18 0.03 0.04 0.95 2002.45 -24.95 NaN 0.11 1.78 0.08 0.62 2.19 0.56 2.85 2.08 0.34 0.04 0.05 1.10 2002.44 -24.24 NaN 0.22 1.11 0.10 2.00 15.10 0.52 2.31 3.19 0.13 0.05 0.06 1.10 2002.43 -21.96 NaN 0.29 1.11 0.14 1.45 10.37 0.60 2.51 3.20 0.11 0.06 0.07 1.10 2002.41 -22.80 NaN 0.10 0.45 0.04 0.49 1.48 0.17 0.59 1.01 0.03 0.07 0.08 1.10 2002.40 -21.45 NaN 0.08 0.37 0.03 0.27 1.25 0.15 0.38 0.92 0.00 0.08 0.10 1.50 2002.38 -25.08 NaN 0.60 0.71 0.11 1.95 5.99 1.24 2.16 3.02 0.12 0.10 0.11 1.50 2002.37 -28.35 NaN 0.62 0.80 0.11 2.61 13.95 0.99 1.33 3.17 0.11 0.11 0.13 1.90 2002.34 -33.97 NaN 0.35 0.18 0.02 0.17 0.52 0.41 0.31 0.46 0.00 0.13 0.15 1.90 2002.32 -34.47 NaN 0.40 0.15 0.04 0.18 0.45 0.46 0.31 0.48 0.00 0.15 0.17 1.90 2002.30 -33.78 NaN 0.31 0.08 0.01 0.16 0.43 0.36 0.32 0.48 0.00 0.17 0.19 1.90 2002.27 -29.17 NaN 0.20 0.13 0.04 0.24 0.64 0.36 2.26 0.48 0.00 0.19 0.21 1.90 2002.25 -28.61 NaN 0.09 0.11 0.02 0.07 0.30 0.20 1.45 0.50 0.08 0.21 0.23 1.90 2002.23 -32.00 NaN 0.46 0.17 0.03 0.31 0.68 0.64 0.91 0.70 0.00 0.23 0.25 2.00 2002.20 -31.66 NaN 0.23 0.35 0.03 0.19 0.33 0.39 0.80 1.06 0.00 0.25 0.27 2.00 2002.18 -26.12 NaN 0.39 0.07 0.02 0.24 0.25 0.43 0.16 0.36 0.00 0.27 0.29 2.00 2002.16 -28.23 NaN 1.30 0.13 0.03 0.58 0.40 1.51 0.20 0.40 0.00 0.29 0.31 2.00 2002.13 -29.58 NaN 0.21 0.09 0.01 0.35 0.34 0.39 0.68 0.23 0.00 0.31 0.33 2.00 2002.11 -27.72 NaN 0.11 0.12 0.02 0.13 0.14 0.27 0.56 0.20 0.00 0.33 0.35 2.00 2002.08 -27.27 NaN 0.03 0.03 0.00 0.11 0.21 0.07 0.26 0.23 0.00 0.35 0.37 2.00 2002.06 -27.03 NaN 0.08 0.05 0.01 0.09 0.12 0.18 1.08 0.19 0.00 0.37 0.39 2.00 2002.04 -27.63 NaN 0.08 0.13 0.02 0.04 0.11 0.24 1.56 0.27 0.00 0.39 0.41 1.95 2002.01 -28.60 NaN 0.15 0.05 0.01 0.13 0.64 0.18 0.32 0.25 0.00 0.41 0.43 1.95 2002.00 -31.84 NaN 0.82 0.11 0.02 0.66 0.97 1.00 0.44 0.56 0.00 0.43 0.44 1.95 2001.96 -31.38 NaN 0.82 0.15 0.03 2.26 3.64 0.95 0.74 1.00 0.00 0.44 0.46 1.95 2001.95 -29.75 NaN 0.14 0.13 0.01 0.31 1.16 0.25 0.86 0.54 0.00 0.46 0.49 2.20 2001.93 -29.22 NaN 0.04 0.13 0.01 0.11 0.30 0.08 0.14 0.49 0.05 0.49 0.51 2.20 2001.91 -30.79 NaN 0.06 0.14 0.01 0.19 0.31 0.09 0.31 0.51 0.00 0.51 0.53 2.20 2001.89 -30.81 NaN 0.42 0.08 0.01 0.26 0.49 0.48 0.21 0.35 0.00 0.53 0.55 2.20 2001.87 -30.06 NaN 0.69 0.11 0.02 0.33 0.33 0.78 0.16 0.35 0.00 0.55 0.57 2.20 2001.85 -30.46 NaN 0.22 0.15 0.01 0.54 0.87 0.27 0.32 0.51 0.00 0.57 0.60 2.20 2001.83 -29.95 NaN 0.12 0.12 0.01 0.35 0.50 0.17 0.26 0.49 0.00 0.60 0.62 2.10 2001.81 -29.54 NaN 0.26 0.20 0.05 0.31 1.18 0.86 0.92 0.87 0.00 0.62 0.64 2.10 2001.79 -27.29 NaN 0.11 0.46 0.02 0.40 0.73 0.32 1.42 1.48 0.00 0.64 0.66 2.10 2001.77 -26.00 NaN 0.11 0.25 0.02 0.12 0.52 0.21 0.45 0.62 0.00 0.66 0.68 2.10 2001.75 -24.68 NaN 0.11 0.35 0.02 0.26 0.63 0.26 0.94 1.05 0.00 0.68 0.70 2.10 2001.73 -22.76 NaN 0.11 0.46 0.02 0.40 0.73 0.32 1.42 1.48 0.00 0.70 0.72 2.10 2001.71 -23.38 NaN 0.11 0.25 0.02 0.12 0.52 0.21 0.45 0.62 0.00 0.83 0.90 7.11 2001.60 -24.62 NaN 0.20 0.66 0.06 0.41 1.21 0.11 0.10 0.07 0.01 0.90 0.96 5.52 2001.53 -26.48 -207.2 0.32 0.46 0.16 1.20 2.18 0.16 0.12 0.18 0.03 0.96 1.07 11.35 2001.50 -25.10 -193.6 0.24 0.30 0.02 0.31 0.53 0.58 0.14 0.23 0.05 1.07 1.17 9.76 2001.44 -24.35 -189.5 0.36 0.51 0.06 0.51 1.35 0.20 0.16 0.21 0.05 1.17 1.23 6.58 2001.39 -26.48 -203.8 0.26 1.23 0.15 0.23 1.12 0.17 0.22 0.27 0.05 1.23 1.30 6.58 2001.34 -27.20 -208.3 0.22 1.31 0.10 0.13 0.73 0.17 0.22 0.24 0.01 1.30 1.39 9.09 2001.27 -27.33 -209.0 0.46 0.56 0.07 0.49 2.21 0.24 0.35 0.68 0.07 1.39 1.47 8.01 2001.21 -25.94 -199.9 0.65 0.30 0.03 0.48 1.24 0.33 0.26 0.60 0.03 1.47 1.55 8.01 2001.15 -23.47 -178.3 0.32 0.23 0.02 0.18 0.42 0.40 0.17 0.38 0.01 1.55 1.63 8.01 2001.09 -26.04 -196.2 0.35 0.26 0.03 0.24 0.73 0.18 0.14 0.34 0.02 1.63 1.71 8.01 2001.02 -28.87 -221.1 0.32 0.16 0.02 0.21 0.67 0.17 0.17 0.31 0.01 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12.50 11.00 1993.38 -23.80 -177.1 0.09 0.26 0.02 0.62 2.01 0.31 1.89 1.42 0.08 12.50 12.60 10.34 1993.32 -24.86 -186.3 0.10 0.23 0.02 1.50 3.11 0.23 0.72 1.99 0.00 12.60 12.70 9.02 1993.26 -25.01 -191.4 0.11 0.33 0.03 0.59 2.23 0.30 0.37 0.90 0.06 12.70 12.77 7.70 1993.21 -25.93 -200.0 0.12 0.22 0.01 0.24 0.80 0.17 0.30 0.49 0.05 12.77 12.86 8.36 1993.17 -27.40 -209.8 0.30 0.22 0.02 0.69 1.43 0.42 0.53 0.99 0.05 12.86 12.91 5.72 1993.13 -27.95 -211.5 0.27 0.23 0.02 1.36 2.69 0.34 0.53 1.06 0.08 12.91 13.00 9.02 1993.10 -28.18 -212.7 0.55 0.34 0.09 5.72 10.38 0.49 0.60 1.05 0.10 13.00 13.09 9.02 1993.05 -28.25 -214.5 0.64 0.34 0.03 1.42 2.78 0.66 0.51 0.80 0.06 13.09 13.20 10.32 1993.00 -28.32 -209.3 1.92 0.44 0.07 1.83 2.88 1.86 0.50 1.31 0.00 13.20 13.30 10.32 1992.96 -29.12 -202.0 0.38 0.28 0.04 1.00 1.94 0.44 0.53 0.89 0.00 13.30 13.40 10.32 1992.88 -27.24 -202.8 0.24 0.23 0.02 3.54 5.14 0.32 0.51 0.94 0.05 13.40 13.51 10.32 1992.80 -26.65 -199.2 0.76 0.27 0.03 2.76 4.62 0.81 0.59 1.35 0.07 13.51 13.57 6.42 1992.72 -25.83 -192.4 0.40 0.22 0.02 1.49 3.38 0.53 0.76 1.61 0.07 13.57 13.63 5.77 1992.66 -24.89 -184.7 0.43 0.40 0.03 2.13 3.61 0.64 1.06 2.10 0.09 13.63 13.71 8.58 1992.62 -25.00 -186.8 1.01 0.35 0.05 5.17 9.82 1.37 1.25 2.54 0.30 13.71 13.80 8.58 1992.50 -24.68 -189.4 0.17 0.38 0.02 1.79 4.21 0.52 1.13 2.50 0.12 13.80 13.88 7.92 1992.49 -26.14 NaN 0.04 0.20 0.01 0.72 1.40 0.18 0.70 0.69 0.06 13.88 13.96 7.92 1992.45 -25.06 -196.5 0.08 0.53 0.02 0.56 1.63 0.18 0.58 0.95 0.00 13.96 14.04 7.92 1992.41 -27.18 -211.9 0.15 0.50 0.04 0.57 1.84 0.25 0.65 1.46 0.00 14.04 14.12 7.92 1992.36 -28.39 -218.6 0.42 0.33 0.06 0.72 2.33 0.44 0.60 1.57 0.05 14.12 14.20 7.92 1992.32 -27.52 -212.4 0.45 0.26 0.04 0.71 2.02 0.33 0.46 1.04 0.06 14.20 14.27 7.92 1992.28 -25.02 -190.5 0.82 0.18 0.03 0.47 0.82 0.92 0.33 0.92 0.00 14.27 14.36 8.58 1992.24 -23.32 -177.6 0.13 0.26 0.02 0.24 0.67 0.19 0.81 0.75 0.00 14.36 14.43 6.74 1992.20 -23.74 -183.0 0.03 0.19 0.01 0.04 0.14 0.04 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5.05 8.12 0.90 2.45 0.10 15.25 15.32 7.13 1991.60 -20.72 -146.3 2.41 0.50 0.07 1.64 2.47 3.12 0.76 1.72 0.10 15.32 15.39 7.13 1991.50 -21.10 -157.8 0.08 0.19 0.02 0.39 0.58 0.17 0.36 0.74 0.07 15.39 15.46 7.13 1991.44 -21.88 -166.1 0.04 0.62 0.02 0.68 1.83 0.19 1.18 1.50 0.22 15.46 15.54 7.13 1991.38 -22.23 -169.7 0.04 0.53 0.03 1.02 2.56 0.19 0.91 0.89 0.11 15.54 15.61 7.13 1991.33 -24.53 -192.6 0.04 1.03 0.04 0.70 1.77 0.19 1.02 0.56 0.07 15.61 15.68 7.13 1991.28 -25.37 -197.8 0.04 0.58 0.02 0.45 0.90 0.14 0.27 0.18 0.11 15.68 15.75 7.13 1991.23 -26.10 -204.5 0.21 0.43 0.03 0.49 1.02 0.33 0.36 0.42 0.07 15.75 15.82 7.13 1991.18 -27.33 -209.5 0.24 0.44 0.03 0.93 2.68 0.30 0.63 1.26 0.17 15.82 15.88 5.73 1991.13 -28.76 -214.9 0.57 0.28 0.12 0.64 2.92 0.43 0.77 0.84 0.11 15.88 15.95 6.97 1991.09 -28.37 -212.8 0.94 0.25 0.03 0.69 1.76 1.76 0.84 1.29 0.00 15.95 16.02 6.97 1991.04 -27.93 -210.8 0.42 0.17 0.02 0.42 1.47 0.54 1.00 0.83 0.09 16.02 16.09 6.97 1991.00 -30.10 -224.9 0.13 0.38 0.03 0.53 2.33 0.34 0.97 1.39 0.18 16.09 16.18 9.04 1990.91 -31.22 -234.7 0.20 0.16 0.01 0.29 0.87 0.26 0.60 0.49 0.00 16.18 16.25 6.97 1990.86 -31.76 -238.0 0.29 0.16 0.01 0.44 1.17 0.44 0.72 0.69 0.00 16.25 16.30 5.59 1990.81 -31.58 -227.3 1.35 1.22 0.12 1.29 7.95 1.74 2.40 5.05 0.47 16.30 16.37 6.97 1990.78 -28.96 -217.8 0.62 0.60 0.03 0.24 1.05 0.68 0.59 0.81 0.00 16.37 16.44 6.97 1990.73 -26.60 -199.1 0.58 0.49 0.18 0.49 1.28 0.63 0.47 1.18 0.06 16.44 16.50 5.59 1990.69 -24.45 -180.9 0.53 0.43 0.06 0.57 1.16 0.57 0.55 1.55 0.00 16.50 16.56 6.28 1990.65 -22.85 -169.6 0.61 0.28 0.02 0.50 0.85 0.83 0.39 1.97 0.00 16.56 16.65 8.35 1990.61 -21.68 -164.4 1.02 0.29 0.01 0.07 0.23 0.99 0.33 0.41 0.00 16.65 16.71 6.32 1990.56 -20.98 -158.8 0.31 0.44 0.05 0.28 0.41 0.28 0.34 0.66 0.00 16.71 16.80 9.16 1990.52 -20.55 -153.1 0.06 0.38 0.01 0.50 1.10 0.27 0.59 1.58 0.15 16.80 16.88 8.45 1990.50 -20.53 -153.3 0.05 0.45 0.02 0.14 0.84 0.42 1.32 2.39 0.14 16.88 16.94 5.61 1990.46 -21.12 -157.3 0.28 0.40 0.04 0.29 1.42 0.60 0.60 1.95 0.19 16.94 17.00 6.32 1990.41 -21.43 -163.8 0.04 0.29 0.01 0.23 1.69 0.20 0.91 1.42 0.13 17.00 17.07 7.03 1990.36 -23.17 -176.5 0.03 0.72 0.04 1.49 3.54 0.30 0.97 0.67 0.00 17.07 17.14 7.03 1990.31 -24.79 -189.1 0.22 0.42 0.03 0.75 1.64 0.34 0.40 0.40 0.00 17.14 17.20 5.61 1990.25 -25.41 -195.9 0.13 0.22 0.01 0.80 2.49 0.43 0.45 0.51 0.00 17.20 17.28 7.74 1990.21 -25.51 -195.9 0.26 0.29 0.02 0.42 1.41 0.82 0.45 0.99 0.04 17.28 17.35 7.03 1990.15 -27.25 -208.5 0.41 0.37 0.04 0.63 1.40 1.22 0.55 1.15 0.05 17.35 17.43 8.46 1990.09 -27.86 -210.4 1.03 0.28 0.04 1.15 2.25 4.46 0.57 2.50 0.00 17.43 17.52 8.46 1990.00 -26.45 -199.2 1.87 0.44 0.05 0.68 0.90 2.88 0.82 1.86 0.00 17.52 17.59 7.06 1989.98 -26.20 -197.4 0.55 0.44 0.04 1.19 3.68 9.49 0.61 3.80 0.00 17.59 17.67 7.76 1989.95 -25.44 -193.7 0.34 0.24 0.03 0.64 1.93 1.97 0.97 1.64 0.06 17.67 17.72 5.66 1989.91 -25.63 -193.2 0.09 0.14 0.01 0.32 0.55 0.62 0.77 0.74 0.00 17.72 17.81 8.46 1989.89 -26.34 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1989.34 -23.66 -205.2 0.12 0.12 0.01 0.49 1.31 0.19 0.33 0.41 0.00 18.74 18.81 7.63 1989.25 -25.15 -218.2 0.33 0.19 0.01 0.29 0.56 0.37 0.40 0.30 0.00 18.81 18.90 9.01 1989.17 -24.64 -216.1 0.71 0.17 0.02 0.44 0.98 0.82 0.43 0.67 0.00 18.90 18.99 8.32 1989.08 -23.51 -203.3 0.50 0.15 0.01 0.30 0.51 0.60 0.39 0.36 0.00 18.99 19.06 7.40 1988.99 -22.83 -196.1 0.17 0.18 0.01 0.30 0.71 0.32 0.56 0.86 0.00 19.06 19.13 7.40 1988.92 -21.77 -184.7 0.22 2.48 0.09 0.78 1.34 0.51 3.88 2.57 0.00 19.13 19.21 7.40 1988.84 -21.21 -182.5 0.11 0.27 0.01 0.22 0.65 0.21 0.60 0.96 0.00 19.21 19.28 7.40 1988.76 -21.32 -185.2 0.15 0.15 0.01 0.22 0.63 0.21 0.53 0.44 0.00 19.28 19.37 8.94 1988.68 -21.76 -184.9 0.17 0.40 0.02 0.26 1.21 0.33 0.68 1.08 0.00 19.37 19.44 7.40 1988.59 -22.88 -195.6 0.55 0.61 0.05 1.41 4.35 0.97 1.84 2.56 0.22 19.44 19.52 7.40 1988.50 -21.22 -182.3 0.02 0.26 0.01 3.49 5.48 0.24 2.64 0.84 0.14 19.52 19.58 5.86 1988.45 -20.96 -179.1 0.36 0.45 0.02 1.00 2.55 0.87 1.45 1.89 0.10 19.58 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0.00 20.52 20.61 8.76 1987.88 -23.94 -208.6 1.94 0.16 0.01 0.21 0.76 2.22 0.45 0.65 0.00 20.61 20.68 7.27 1987.82 -23.54 -205.0 0.56 0.14 0.04 0.54 0.42 0.68 0.34 1.16 0.00 20.68 20.75 6.55 1987.77 -22.62 -198.6 0.56 0.24 0.03 0.26 0.36 0.61 0.38 1.55 0.00 20.75 20.82 7.27 1987.73 -21.84 -188.7 0.23 0.21 0.03 0.29 0.59 0.31 1.08 1.42 0.00 20.82 20.91 8.71 1987.68 -21.09 -180.0 0.65 0.30 0.02 0.37 1.03 0.83 0.71 1.03 0.00 20.91 20.99 8.71 1987.62 -21.59 -188.7 0.03 0.21 0.02 0.32 0.39 0.08 0.35 0.33 0.00 20.99 21.09 9.43 1987.56 -20.64 -181.1 0.24 0.14 0.00 0.09 0.16 0.36 0.75 0.65 0.06 21.09 21.18 9.43 1987.50 -19.13 -161.5 0.02 0.18 0.06 0.33 0.72 0.13 0.74 0.84 0.00 21.18 21.25 7.27 1987.39 -19.45 -167.4 0.03 0.25 0.01 0.09 0.42 0.28 1.37 1.30 0.00 21.25 21.33 7.27 1987.33 -21.29 -187.8 0.05 0.15 0.01 0.26 0.88 0.25 0.71 0.50 0.00 21.33 21.40 7.27 1987.27 -22.17 -199.5 0.02 0.19 0.01 0.19 1.43 0.19 1.24 0.74 0.11 21.40 21.49 8.80 1987.22 -23.08 -205.7 0.44 0.60 0.02 0.70 1.05 0.49 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