Program and Abstracts
Third International Symposium on the Arctic Research(ISAR-3)-

Detecting the change in the Arctic system and searching the global influence –January 14-17, 2013
Miraikan (7th Floor)
National Museum of Emerging Science and Innovation
Tokyo, Japan
Organized by

National Committee of IASC, Subcommittee for International Affairs, Committee on Earth and Planetary
Sciences, Science Council of Japan
Japan Consortium for Arctic Environmental Research (JCAR)

Co-Organized by
IFES-GCOE, Hokkaido University
International Arctic Research Center (IARC)
Japan Agency for Marine-Earth Science and Technology (JAMSTEC)
National Institute of Polar Research (NIPR)

Supported byCenter for Computational Sciences (CCS), University of Tsukuba
Climate and Cryosphere Project (CliC), World Climate Research Programme (WCRP)International Arctic Science Committee (IASC)
Research Institute for Humanity and Nature (RIHN)

Symposium Organizing Committee
Chair: Tetsuo OHATA, RIGC,JAMSTEC (Chair of JCAR)
Co-chair: Atsuko SUGIMOTO, Hokkaido University (Chair of the Japan National Committee for IASC)

Kumiko GOTO-AZUMA (NIPR), Hiroyuki ENOMOTO (NIPR), Tetsuya HIYAMA (RIHN), Masahiro
HORI, (EORC JAXA), Tamotsu IGARASHI (RESTEC), Michiyo YAMAMOTO-KAWAI (TUMSAT),
Yojiro MATSUURA (FFPRI), Takuji NAKAMURA (NIPR), Toru NOZAWA (NIES), Sei-Ichi SAITO(Hokkaido University), Koji SHIMADA (TUMSAT), Konosuke SUGIURA (RIGC, JAMSTEC), Rikie
SUZUKI, (RIGC, JAMSTEC), Hiroshi L. TANAKA (CCS, University of Tsukuba), Jinro UKITA(Niigata University)

International Advisory Committee
Larry HINZMAN, (IARC, USA), Kim HOLMEN (NPI, Norway), Yeadong KIM (KOPRI, Korea),
Atsumu OHMURA (ETH, Switzerland), Volker RACHOLD (IASC, Germany), Konrad STEFFEN (WSL,
Switzerland), John WALSH (IARC, USA), Peter WADHAMS (University of Cambridge, UK), Cunde
XIAO, (CAREERI, CAS, China), Huigen YANG, (PRIC, China)

Program Committee
Chair: Atsuko SUGIMOTO, Hokkaido University
Teruo AOKI (MRI), Hiroyuki ENOMOTO (NIPR), Tetsuya HIYAMA (RIHN), Michiyo
YAMAMOTO-KAWAI (TUMSAT), Toru NOZAWA (NIES), Tetsuo OHATA (RIGC, JAMSTEC),
Atsumu OHMURA (ETH, Switzerland), Sei-Ichi SAITO (Hokkaido University), Kaoru SATO (The
University of Tokyo), Koji SHIMADA (TUMSAT), Rikie SUZUKI (RIGC, JAMSTEC), Shuhei
TAKAHASHI (KIT), Hiroshi L. TANAKA (CCS, University of Tsukuba)

Local Organizing Committee
Chair: Yuji KODAMA, JCAR, NIPR
Takahiro IIDA (NIPR), Yusuke KAWAGUCHI (JAMSTEC), Michiyo YAMAMOTO-KAWAI(TUMSAT), Hideki KOBAYASHI (JAMSTEC), Kohei MIZOBATA (TUMSAT), Kazuhiro NAOKI(JAXA), Yasunobu OGAWA (NIPR), Konosuke SUGIURA (JAMSTEC), Rikie SUZUKI (JAMSTEC),
Takeshi TAMURA (NIPR), Tomonori TANIKAWA (JAXA), Hironori YABUKI (JAMSTEC)The Third International Symposium on the Arctic Research: Detecting thechange in the Arctic system and searching the global influence
Preface

It is our pleasure to welcome you to the Third International Symposium on
Arctic Research (ISAR-3) to be held on January 14 to 17, 2013 at Tokyo. This
Symposium is the third one following the past two Symposium held in November, 2008
(ISAR-1) and December, 2010 (ISAR-2).
The Arctic and surrounding region of sub-Arctic is one key area for the studyof global change since it is showing the strongest warming under the ongoing global
warming. It is affecting the natural system and also has strong influence to the people
living in that region. Moreover, the influence is not only limited to this area, but isalready showing influence to the mid to low latitude, and projected to have global
influence. The scientific discussion about this region will be important for advancementof science, and as basis for the social activities in this region.
In this Symposium, first, we expect papers to discuss on the evidence andcause of changes occurring in the Arctic System, composed of atmosphere, ocean, landsystem and cryosphere, and its interactiona. Secondly, we expect discussions on theinfluence to the wider globe, presently occurring through atmosphere.
The Symposium is formed from 7 general sessions and 6 special sessions, sothat researchers in many disciplines can report, and can also discuss on narrow timely
topics. We hope that discussion made in the Symposium will lead to some new idea andresearch to be made in the future.
On behalf of the Symposium Organizing Committee of the ISAR-3, I
sincerely appreciate the presence of all attendants and hope of the continuous
participation to ISAR.
January, 2013.
Tetsuo Ohata
Chair of the ISAR-3 Organizing Committee
Japan Agency for Marine-Earth Science and Technology#. 
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Program for the Third International Symposium on the Arctic Research(ISAR-3)
January 14-17, 2013, Miraikan, Tokyo, Japan
January 14, 2013 (Monday)
14:00-16:15 Public lecture (in Japanese language)

January 15, 2013 (Tuesday), MiraiCan Hall
9:15-

Registration

10:00-10:30

Opening Session

Chair: Yuji Kodama

Welcome Speeches
Tetsuo Ohata (Chair of ISAR-3 Organizing Committee)
Volker Rachold (Executive Secretary, IASC)TBD (Ministry of Education, Culture, Sports, Science & Technology)
Kazuyuki Shiraishi (Director, NIPR)
Page
10:30 – 12:00
Keynote speech
KN-1
INTENSIFIED WARMING OF THE ARCTIC:
CAUSES AND IMPACTS ON MIDDLE LATITUDES
J. E. Walsh
KN-2
ARCTIC WARMING AND ITS CONSEQUENCES FOR PERMAFROST
H.-W. Hubberten， J. Boike， H. Lantuit
KN-3
CATASTROPHIC REDUCTION OF SEA-ICE IN THE ARCTIC OCEAN - ITS IMPACT
ON THE MARINE ECOSYSTEMS IN THE POLAR REGIONN. Harada， K. Kimoto， J. Onodera， E. Watanabe， M. Honda， M.J. Kishi，
S. Chiba， T. Kikuchi， Y. Tanaka， M. Sato， K. Saruwatari， F. Ito，
Y. Shiraiwa， K. Matsuno， A. Yamaguchi
12:00-

Photo, Lunch

13:30-14:45 Poster session

G1 (P1-P10), G5, S5 at Conference room 3

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Oral session
January 15, 2013 (Tuesday), MiraiCan Hall
14:45-18:40
G1-O1
G1-O2
G1-O3

G1-O4
G1-O5
G1-O6
G1-O7

(G1) Atmospheric science
Chair: Kaoru SATO, John WALSH
ATMOSPHERIC REMOTE SENSING IN THE ARCTIC BY INCOHERENT SCATTERTECHNIQUE USING THE EISCAT AND EISCAT 3D RADARS
E. Turunen (Invited)
POLAR IONOSPHERE AND THERMOSPHERE COOLING OVER THE PAST 30
YEARS
Y. Ogawa， T. Motoba， I. Häggström， S. Nozawa， S. C. Buchert
CHARACTERISTICS OF THE MESOSPHERIC GRAVITY WAVES DERIVED FROMOH AIRGLOW IMAGES AT TROMSOE, NORWAY
S. Oyama， M. Ejiri， S. Suzuki， K. Shiokawa， T. Nakamura， M. Tsutsumi，
Y. Tomikawa， T. T. Tsuda， S. Nozawa， T. Takahashi
UPPER ATMOSPHERIC OBSERVATION AT RESOLUTE CANADAQ. Wu
STUDIES OF VERTICAL COUPLING PROCESSES IN THE ARCTIC REGION USING
A GCM
Y. Miyoshi， T. Nakamura，Y. Ogawa，Y. Tomikawa，H. Fujiwara
INTERHEMISPHERIC DIFFERENCES ON THE WINTER POLE-EQUATOR
CONNECTION IN THE UPPER STRATOSPHERE/LOWER MESOSPHERE
K. Okamoto， K. Sato， S. Watanabe
ANALYSIS OF VERTICAL PROFILES OF CO2, CH4, SF6 IN THE ARCTICATMOSPHERE
P. Patra， S. Wofsy， Members ACTM， Members HIPPO

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6

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9
10

16:35-16:50 Coffee break
G1-O8
G1-O9
G1-O10G1-O11G1-O12
G1-O13

G1-O14SIMULTANEOUS OCCURRENCE OF POLAR STRATOSPHERIC CLOUDS AND
UPPER-TROPOSPHERIC CLOUDS CAUSED BY BLOCKING ANTICYCLONES
M. Kohma， K. Sato
PROJECTED CHANGES IN ARCTIC SUMMER STORM-TRACK ACTIVITY BY
CMIP3 CLIMATE MODELS
K. Nishii， H. Nakamura， Y. J. Orsolini
INTERANNUAL VARIABILITY OF THE EAST ASIAN WINTER MONSOON
K. Takaya， H. Nakamura
ARCTIC OSCILLATION AND EAST ASIAN CLIMATE CHANGE
S. J. Kim， B.M. Kim， J. H. Jeong， S. H. Woo，T. Shim， H. Choi
IMPACT OF ARCTIC SEA-ICE RETREAT ON THE RECENT CHANGE IN
CLOUD-BASE HEIGHT DURING AUTUMN
K. Sato， J. Inoue， Y. -M. Kodama， J. E. Overland
PAN EURASIAN EXPERIMENT (PEEX) TOWARDS A NEW MULTINATIONALENVIRONMENT AND CLIMATE RESEARCH EFFORT IN EURASIA
M. Kulmala， H. Lappalainen， T. Petaja， M. Sipila， S. Sorvari，P. Alekseychik， M. Paramonov，V. Kerminen， S. Zilitinkevich
ENHANCED POLEWARD ATMOSPHERIC MOISTURE TRANSPORT AMPLIFIESNORTHERN HIGH-LATITUDE WETTING TREND
X. Zhang， J. He， J. Zhang， I. Polyakov，R. Gerdes， J. Inoue， P. Wu

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January 15, 2013 (Tuesday), Conference Room 2
14:45-16:00(S5) GRENE Arctic project
Chair: Hiroyuki ENOMOTO, Takashi YAMANOUCHI

S5-O1
S5-O2
S5-O3
S5-O4

S5-O5

GRENE-ARCTIC CLIMATE CHANGE RESEARCH PROJECT: STRATEGY AND
IMPLEMENTATION
H. Enomoto, T. Yamanouchi
ARCTIC CHALLENGE - OUR RESEARCH STRATEGY FOR ARCTIC CLIMATECHANGE
T. Nozawa， A. Sugimoto， J. Ukita， H. Enomoto， S. Aoki
HOW VEGETATION CHANGE CONTRIBUTE TO POLAR AMPLIFICATION IN
WARM CLIMATE?
R. O'ishi， A. Abe-Ouchi
COMPARISON OF XCO2 SIMULATED BY NIES TRANSPORT MODEL AND
OBSERVED BY GOSAT IN POLAR REGIONS
D. Belikov， A. Bril， F. Chevallier， S. Maksyutov， S. Oshchepkov， T. Saeki，
H. Takagi
FORECAST OF SUMMER SEA-ICE EXTENT IN THE ARCTIC BASED ON WINTER
ICE MOTION
N. Kimura， A. Nishimura， H. Yamaguchi

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16:00-16:15 Coffee break
16:15-18:25 (G5) Terrestrial ecosystem
Chair: Rikie SUZUKI, Walter OECHEL
G5-O1
G5-O2

G5-O3

G5-O4
G5-O5
G5-O6

G5-O7
G5-O8

CROSS-DISCIPLINARY RESEARCH COLLABORATION FOR EARLY DETECTION
OF BIOLOGICAL FEEDBACKS
N. Saigusa， R. Suzuki， T. Hiyama， K. Hayashi
LONG TERM VARIABILITY OF CARBON IN PERMAFROST-DOMINATEDECOSYSTEMS
T. Maximov， H.Dolman， J.Huissteden， T.Ohta， A.Sugimoto， A.Kononov，
A.Maksimov， R.Pertov， M.Terentyeva (Invited)
ESTIMATING LARGE SCALE, REGIONAL, NET CO2 AND CH4 FLUXES USINGNESTED TOWER, AIRCRAFT FLUX, REMOTE SENSING, AND MODELINGAPPROACHES
W. Oechel, D. Zona, C. Sturdevant (Invited)
BACTERIAL DIVERSITY AND CHEMICAL COMPOSITION OF PERMAFROSTSOILS OF NY-ALESUND, ARCTIC
S. M. Singh(CANCELLED)
IMPACT OF CLIMATE CHANGE ON ECOSYSTEM FUNCTIONING AND GHG
EMISSION IN ARCTIC TUNDRA ACROSS MULTIPLE SCALES
D. Zona， W. Oechel
REMOTE SENSING OF DECIDUOUS SHRUBS AND PHYTOMASS IN ALASKAN
ARCTIC TUNDRA
K. Kushida， S. Hobara， S. Tsuyuzaki， Y. Kim， M. Watanabe， K. Harada，
G. R. Shaver， M. Fukuda
THE CLIMATIC EFFECT TO NORTH EURASIA ECOSYSTEMS. ANALYSIS OF
30-YEARS SATELLITE DATA.
V. Elsakov
GROUND-TRUTH FOR SATELLITE OBSERVATION BY PERFORMING DAILYFIELD STUDIES IN AN OPEN-CANOPY BLACK SPRUCE FOREST IN ALASKA
AND A CLOSED-CANOPY EVERGREEN CONIFEROUS FOREST IN JAPANS. Nagai， T. Nakai， T.M. Saitoh， R.C. Busey， H. Kobayashi， R. Suzuki，H. Muraoka， Y. Kim

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January 16, 2013 (Wednesday),
9:00-

Miraican Hall

RegistrationPage

9:30-11:05(S2) Changes in water and carbon cycles of terrestrial ecosystem on permafrost
in a warming Arctic
Chair: Atsuko SUGIMOTO, Jacobus van HUISSTEDEN

S2-O1

ACCELERATION OF THE ARCTIC WATER CYCLE: EVIDENCE FROM THE LENA
BASIN, SIBERIA
J. Cherry， V. Alexeev， V. Romanovsky (Invited)
RECENT VEGETATION FIRE INCIDENCE IN RUSSIA
H. Hayasaka
VEGETATION GROWTH AND METHANE EMISSION AT TAIGA-TUNDRABOUNDARY ECOSYSTEM IN EASTERN SIBERIA
A. Sugimoto， R. Shingubara， I. Bragin， G. Iwahana， M. Nakamura， S. Tei，
M. Liang， S. Takano， R. Pedrov， T. Maximov
THAW LAKE EVOLUTION AND LONG TERM CARBON EMISSION FROMPERMAFROST.
J. van Huissteden
UPSCALING OF METHANE FLUXES FROM ARCTIC WETLANDS USINGPEATLAND-VU MODEL AND FOOTPRINT MODELING
A. Budishchev， Y. Mi， J. van Huissteden， G. Schaepman-Strub，
F. J. Parmentier， G. Fratini， L. Belelli-Marchesini， A. Gallagher，A. J. Dolman， T. C. Maximov
CH4 AND N2O DYNAMICS OF A LARIX GMELINII FOREST IN CONTINUOUS
PERMAFROST REGION OF CENTRAL SIBERIA
T. Morishita， Y. Matsuura， T. Kajimoto， A. Osawa， O. Zyryanova，A. Prokushkin

S2-O2
S2-O3

S2-O4
S2-O5

S2-O6

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11:05-11:20 Coffee break
11:20-12:15(G3) Hydrology, permafrost and snow cover I
Chair: Tetsuya HIYAMA, Larry HINZMAN

G3-O1

GROUND THERMAL REGIME AND ACTIVE LAYER THICKNESS MONITORING
AND MODELLING IN THE NORDIC AREA
B. Etzelmüller， H. H. Christiansen， K. Gisnas， K. Isaksen， T.V. Schuler，S. Westermann(Invited)
PERMAFROST AND ACTIVELAYER MONITORING NETWORK IN ALASKANCOMMUNITIESK. Yoshikawa， K. Harada， G. Iwahana， J. Khalilova (Invited)
THERMAL STATES OF MONGOLIAN PERMAFROST AND DEPLOYINGPERMAFROST OBSERVATORIES OVER THE ARCTIC
M. Ishikawa， K. Yoshikawa， Y. Jambaljav， N. Sharkhuu， I. Yamahashi，
S. Westermann， B. Etzelmüller， M.N. Zheleznyak， S. Laxton

G3-O2
G3-O3

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12:15-13:30 Lunch
13:30-14:45 Poster session

G3, G6, S2, S3 at Conference room 3

14:45-16:30(G3) Hydrology, permafrost and snow cover II
Chair: Tetsuya HIYAMA, Larry HINZMAN

G3-O4PERMAFROST MAP IN RUSSIA USING COMMUNITY-BASED PERMAFROSTAND ACTIVE LAYER MONITORING NETWORK
Y. Khalilova， D. Sergeev， K. Yoshikawa
PARAMETRIZATIONOFRUNOFFFORMATIONMECHANISMSIN
MOUNTAINOUS PERMAFROST CONDITIONS OF RUSSIA AND CANADA (THEKOLYMA WATER BALANCE STATION AND THE WOLF CREEK RESEARCH
WATERSHED)
O. Semenova， L. Lebedeva (CANCELLED)

G3-O5

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G3-O6
G3-O7

G3-O8
G3-O9
G3-O10

TEMPORAL SEQUENCING OF ANNUAL SPRING RUNOFF IN FOUR MAJOR
ARCTIC-DRAINING RIVERS
R. Ahmed， T. D. Prowse, Y. B. Dibike， B. R. Bonsal
ICE MOVEMENT IN THE LENA RIVER AND THE TYPOLOGY OF SPRING
FLOODING: AN INTERPRETATION OF LOCAL SOURCES INTEGRATED WITH
SATELLITE IMAGERY USING A MULTIDISCIPLINARY APPROACH
H. Takakura， Y. Yoshikawa， M. Watanabe， T. Sakai， T. Hiyama
WATER BALANCE OF ARCTIC WETLANDS WITH DIFFERING ICE WEDGEPOLYGON TYPE
A. Liljedahl， R. Daanen， C. Wilson, J. Schulla， L. Hinzman
VEGETATION WATER USE COMPARISON IN A SUB-ARCTIC, BOREAL FOREST
ENVIRONMENT USING HYDROGRAPH ANALYSIS
W. R. Bolton， J. M. CableICE COVER OF EURASIAN LAKES AND INLAND SEAS FROM SATELLITE AND
IN SITU OBSERVATIONS
A. Kouraev， M. Shimaraev， F. Rémy， M. Naumenko， A. Suknev

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16:30-16:45 Coffee break
16:45-17:55(S3) Changes in the Greenland ice sheet in the context of interactions
with the atmosphere and the ocean
Chair: Teruo AOKI, Shin SUGIYAMA

S3-O1

A UNIFIED VIEW OF THE GREENLAND FLOW DISTORTION AND ITS IMPACT
ON BARRIER FLOW, TIP JETS AND COASTAL OCEANOGRAPHY
G. W. K. Moore (Invited)
BIOGENIC IMPURITIES DARKENING THE GREENLAND ICESHEETN. Takeuchi， N. Nagatsuka， R. Shimada， J. Uetake (Invited)
ICE MASS LOSS IN NORTHWESTERN GREENLAND
S. Sugiyama， S. Matoba， S. Yamaguchi， D. Sakakibara， S. Matsuno
SENSITIVITY OF RESPONSE OF GREENLAND ICE SHEET TO GLOBALWARMING ON SURFACE MASS BALANCE PARAMETERIZATION AND
REFERENCE CLIMATE STATES
S. Fuyuki， A. Abe-Ouchi， K. Takahashi

S3-O2
S3-O3
S3-O4

18:30-

Banquet at Hotel Nikko Tokyo, Banquet Room Apollon

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January 16, 2013 (Wednesday), Conference Room 2
9:00-

RegistrationPage

9:30-11:40(G6) Marine ecosystem
Chair: Sei-Ichi SAITO, Sang H. LEE

G6-O1
G6-O2
G6-O3
G6-O4

PHYTOPLANKTON PIGMENTS IN CHUKCHI SEA DURING AUGUST TOSEPTEMBER 2010，
H. Jin， J. Chen， H. Li， S. Gao， Y. Lu， Y. Zhuang (Invited) (CANCELLED)SATELLITE REMOTE SENSING OF PRIMARY PRODUCTIVITY IN THE BERINGAND CHUKCHI SEAS USING AN ABSORPTION-BASED APPROACH
T. Hirawake， K. Shinmyo， A. Fujiwara， S. Saitoh (Invited)
MACROMOLECULAR PRODUCTION OF PHYTOPLANKTON IN THE NORTHERN
BERING SEA, 2007
H. T. Joo， J. H. Lee， C. K. Kang， J. H. Lim， S. H. Lee
ISOLATION OF NEW STRAINS OF COCCOLITHOPHORE, EMILIANIA HUXLEYIFROM ARCTIC SEA AND THEIR CHARACTERIZATION
M. Satoh， F. Itoh， K. Saruwatari， N. Harada， I. Suzuki， Y. Shiraiwa

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10:40-10:55 Coffee break
G6-O5

G6-O6
G6-O7

FAUNAL TURNOVER AND SHELL DENSITY CHANGE IN THE ARCTIC SEA:RESPONSES UNDER OCEAN ACIDIFICATION
K. Kimoto， N. Harada， J. Onodera， O. Sasaki， H. Kano， M. Honda，
Y. Tanaka
YEAR-LONG MONITORING OF UNDER-ICE PHYTOPLANKTON ASSEMBLAGESIN THE ARCTIC BY ICE-TETHERED PROFILERS
S. Laney， J. Toole， R. Krishfield， C. Ashjian
SINKING FLUXES OF DIATOM AND SILICEOUS FLAGELLATES IN THE
NORTHWIND ABYSSAL PLAIN
J. Onodera， N. Harada， M. Honda， Y. Tanaka

11:40-12:10(G2) Ocean and sea ice I
Chair: Michiyo YAMAMOTO-KAWAI, Jennifer HUTCHINGS

G2-O1

MONITORING THIN SEA ICE THICKNESS WITH MODIS
Ø. Rudjord， Ø. Due Trier， R. Solberg
ARCTIC SEA ICE FORECASTING SERVICE DURING CHINARE 2012
C. Li， M. Li， X. Wu， Z. Tian， L. Zhang， F. Liu， S. Meng (CANCELLED)

G2-O2

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12:10-13:30 Lunch
12:20-13:20 APECS meeting
13:30-14:45 Poster session

G3, G6, S2, S3 at Conference room 3

14:45-17:55(G2) Ocean and sea ice II
Chair: Michiyo YAMAMOTO-KAWAI, Jennifer HUTCHINGS

G2-O3

SEA-ICE MELT ONSET ASSOCIATED WITH ICE DEFORMATION EVENTSDURING EARLY SUMMER
J. K. Hutchings， Y. Kawaguchi， F. Vivier
HOW DOES THE ARCTIC SUMMER WIND MODULATE OCEAN HEAT BUDGET
IN SEA ICE REDUCTION ZONE?
E. Watanabe， M. Ogi (Invited)
ARCTIC ICE-OCEAN MODELING STRATEGY: HOW TO VERIFY MODELS OF
CLIMATE CHANGE WITH EXISTING DATA
M. Ikeda
RECONSTRUCTION OF WATER CIRCULATION IN THE PACIFIC SECTOR OF
THE ARCTIC OCEAN
G. Panteleev， T. Kikuchi， A. Proshutinsky， J. Zhang

G2-O4
G2-O5
G2-O6

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G2-O7

ARCTIC OCEAN LIQUID FRESHWATER STORAGE TREND 1992-2011
B. Rabe， M. Karcher， F. Kauker， U. Schauer， J. Toole， R. Krishfield，
S. Pisarev， R. Gerdes，T. Kikuchi (Invited)64

16:10-16:25 Coffee break
G2-O8
G2-O9
G2-O10G2-O11
G2-O12G2-O13

18:30-TEMPORAL VARIATION OF OCEAN CURRENT STRUCTURE CAUSED BY SEA
ICE MOTION
D. Hirano， K. Shimada， E. Yoshizawa
ESTIMATION OF VOLUME TRANSPORT AND HEAT FLUX THROUGH BARROWCANYONK. Mizobata， K. Shimada
SHIFTS IN SEA ICE CONDITIONS OF SIBERIAN SHELF SEAS IMPACT THE
HALOCLINE OF THE ARCTIC OCEAN
L. G. Anderson， P. S. Andersson， G. Bjork， E. P. Jones， S. Jutterstrom，I. Wahlstrom
SHOALING OF THE NUTRICLINE WITH AN INCREASE IN NEAR-FREEZINGTEMPERATURE WATER IN THE MAKAROV BASIN
S. Nishino， M. Itoh， W. J. Williams， I. Semiletov
SPATIAL AND TEMPORAL VARIABILITY OF AIR-SEA CO2 EXCHANGE OFALONGSHORE WATERS NEAR BARROW, ALASKA
H. Ikawa， W. C. Oechel
FATE OF TERRESTRIAL COLORED DISSOLVED ORGANIC MATTER (CDOM) IN
THE ARCTIC OCEAN: EXPORTED OR REMOVED?
M. A. Granskog， C. A. Stedmon， P. Dodd

Banquet at Hotel Nikko Tokyo, Banquet Room Apollon

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January 17, 2013 (Thursday),
9:00-

Miraican Hall

RegistrationPage

9:30-11:40
S6-O1
S6-O2
S6-O3
S6-O4

(S6) Monitoring of the Arctic environment
Chair: Atsumu OHMURA, Koji SHIMADAMONITORING OF ENVIRONMENT IN THE ARCTIC
A. Ohmura
THE RAPIDLY CHANGING ARCTIC SEA ICE EXTENT FROM SPACE BASEDAMSR-E AND AMSR2 OBSERVATIONS
M. Hori， K. Imaoka， K. Naoki， M. Seki， J. C. Comiso (Invited)
ESTIMATION OF ARCTIC SEA-ICE THICKNESS FROM SATELLITE PASSIVE
MICROWAVE RADIOMETERS
K. Tateyama， R. A. Krishfield， W.J. Williams， H. Enomoto
MONITORING WARMING IN THE EURASIAN BASIN OF THE ARCTIC OCEAN
I. Polyakov (Invited)

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10:40-10:55 Coffee break

S6-O5

S6-O6

S6-O7

OCEAN WARMING, FRESHENING AND CIRCULATION IN THE PACIFIC SECTOR
OF THE ARCTIC OCEAN,“POSITIVE FEEDBACK MECHANISMS TO DRIVE THE
CATASTROPHIC REDUCTION OF SEA ICE”
K. Shimada， K. Mizobata， E. Yoshizawa， D. Hirano， T. W. Kim， H. K. Ha，
H. J. Lee， H. J. Lee， K. H. Chung， S. H. KangTHE
OPTIMISM
PROJECT(OBSERVINGDYNAMICALAND
THERMODYNAMICALPROCESSES IMPACTING THE SEA-ICE MASSBALANCE FROM IN SITU MEASUREMENTS):CURRENT STATUS AND
FUTURE PLANS.
F. Vivier， A. Lourenco， P. Bouruet-Aubertot， Y. Cuypers， D. Dausse，
L. Eymard， N. Martin， A. Weill， M. Dechambre， F. Bonnefoy， P. Ferrant，L. Gentaz， J-M. Rousset， B. Alessandrini， R. Loisil， H. Barrois，
N. Amarouche， J-M. Panel
DYNAMICS OF THE GROUND TEMPERATURE REGIME IN EAST SIBERIA
M. Zheleznyak

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11:40-12:55 Lunch
12:55-14:10 Poster session

G1 (P11-P18), G2, G4, G7, S1, S4, S6 at Conference room 3

14:10-17:05(S4) International cooperation on Arctic observation and research
Chair: Tetsuo OHATA, Volker RACHOLD

S4-O1

AN OVERVIEW AND PERSPECTIVE ON CHINESE ARCTIC RESEARCH
H. Yang， J. He， X. Zhang， D. Chen， Y. Wang， S. Xu (CANCELLED)
NEW KOREAN BI-POLAR OCEAN PROGRAM (K-PORT, KOREA-POLAR OCEANIN RAPID TRANSITION)
S. H. Kang， K. H. Chung， J. K. Hong， Y. K. Jin
THE PRESENT CONDITION OF ARCTIC ENVIRONMENTAL RESEARCH IN
JAPAN AND THE ROLE OF JCAR
T. Ohata， Y. Kodama
INTRODUCTION OF THE ASIAN FORUM OF POLAR SCIENCE (AFoPS)
A. A. Samah， S. A. Ailas， K. Shiraishi， K. Watanabe， H. Enomoto
NEXT-GENERATIONECOSYSTEMEXPERIMENT(NGEEARCTIC):OPPORTUNITIES FOR INTERNATIONAL COLLABORATION AND PARTNERSHIP
L. D. Hinzman， S. D. Wullschleger， C. J. Wilson， J. C. Rowland，S. S. Hubbard，M. S. Torn，W. J. Riley， D.E. Graham， L. Liang， R. J. Norby，
P. E. Thornton，A. Rogers
INTEGRATED LAND ECOSYSTEM - ATMOSPHERE PROCESSES STUDY (ILEAPS)
T. Suni， M. Kulmala， A. Guenther
INTERACT - ACCESS TO THE ARCTIC
M. Johansson， T. Callaghan

S4-O2
S4-O3
S4-O4
S4-O5

S4-O6
S4-O7

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15:35-15:50 Coffee break
S4-O8
S4-O9
S4-O10S4-O11
S4-O12

17:10-HISTORY AND FUTURE OF THE PACIFIC ARCTIC GROUP (PAG)
J. Grebmeier， J. He， T. Kikuchi， J. Calder
ADDED VALUE THROUGH COOPERATION. THE ROLE OF SVALBARD SCIENCEFORUM AND THE RESEARCH IN SVALBARD DATABASE
H.R. Pedersen, K. Holmén, K. Bælum, K.H. Davidsen
THE ARCTIC MONITORING AND ASSESSMENT PROGRAMME (AMAP)
L.-O. Reiersen
THE SUSTAINING ARCTIC OBSERVING NETWORKS (SAON)
J. R. Larsen
THE INTERNATIONAL POLAR INITIATIVE
V. Ryabinin， D. Hik， J.-G. Winther， V. Rachold

Closing session

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January 17, 2013 (Thursday), Conference Room 2
9:00-

RegistrationPage

9:30-11:40
S1-O1
S1-O2
S1-O3

(S1) Polar (Arctic) amplification in global warming
Chair: Hiroshi L. TANAKA, Vladimir ALEXEEVDOES POLAR AMPLIFICATION HAVE A MAXIMUM IN PRESENT DAY
CLIMATE?
V. Alexeev， C. Jackson (Invited)
ON PROCESSES AND FEEDBACKS OF RELEVANCE TO ARCTICAMPLIFICATION AND CLIMATE CHANGE
W. Maslowski， J. Kinney, R. Osinski， A. Roberts (Invited)
CONTRIBUTING PROCESSES TO ARCTIC TEMPERATURE AMPLIFICATION FOR
A RANGE OF FORCING IN MIROC GCM
M. Yoshimori， M. Watanabe， A. Abe-Ouchi， H. Shiogama， T. Ogura

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10:25-10:40 Coffee break
S1-O4
S1-O5
S1-O6

SIMULATION FOR 20TH AND 21ST CENTURIES WITH A 60KM-MESH GLOBALATMOSPHERIC MODEL
S. Kusunoki， R. Mizuta
DETAILED SURVEY OF A LARGE BAROCLINIC EDDY WITH EXTREMELY HIGHTEMPERATURES IN THE WESTERN CANADA BASIN
Y. Kawaguchi， M. Itoh， S. Nishino
DYNAMICAL ORIGIN OF THE ARCTIC OSCILLATION
H. L. Tanaka

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11:25-12:55 Lunch
12:55-14:10 Poster session
14:10-15:10

G1 (P11-P18), G2, G4, G7, S1, S4, S6 at Conference room 3(G7) Interdisciplinary modeling studies
Chair: Toru NOZAWA

G7-O1

G7-O2
G7-O3
G7-O4

INITIAL RESPONSE OF REDUCED ICE ALBEDO AND INCREASEDGREENHOUSEGASCONCENTRATIONSINCOUPLED
ATMOSPHERE-OCEAN-SEA ICE ECHAM-FESOM SIMULATIONS
T. Semmler， D. Sidorenko， T. Jung
MODELING EXCESS ICE AND THERMOKARST IN THE COMMUNITY LAND
MODEL
H. Lee， S. C. Swenson， D. M. Lawrence， A. G. Slater
IMPACT OF SURFACE WINDS ON OCEAN PROCESSES IN THE NORDIC SEAS
INFERRED FROM THE 1/12-DEGREE ARCTIC OCEAN HYCOM-CICE
D. S. Dukhovskoy， M. A. Bourassa
THE CRYOMET PROJECT - COMBINING DETERMINISTIC AND PROBABILISTICDOWNSCALING TO MODEL SNOW DEPTH OVER A WIDE RANGE OF SCALES
S. Westermann， T. Berntsen， B. Etzelmueller， K. Gisnas， J. O. Hagen，
J. E.Kristjansson， T.V. Schuler， F. Stordal

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15:25-16:45(G4) Ice sheets, glaciers and ice cores
Chair: Shuhei TAKAHASHI, Maria ANANICHEVA

G4-O1

MOUNTAIN GLACIERS OF THE NORTHEASTERN ASIA: NEW ASSESSMENTS
M. Ananicheva (Invited)
ATMOSPHERIC TOXICS DEPOSITION TO SVALBARD: THE EMERGING PICTURE
M. Hermanson， E. Isaksson， C. Teixeira， D. Muir， P. Leonards
NITRATE AND SULFATE ANTHROPOGENIC TRENDS IN THE 20TH CENTURY
FROM FIVE SVALBARD ICE CORES
D. Samyn， C. Vega， H. Motoyama， V. Pohjola

G4-O2
G4-O3

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G4-O4

G4-O5

Added
S4-O13RESPONSE OF GLACIER “ELA” IN SUNTAR-KHAYATA, EASTERN SIBERIA, ON
CLIMATE CHANGE
S. Takahashi， T. Shirakawa， T. Kadota， H. Yabuki， K. Konya， T. Ohata，
H. Enomoto，N. Takeuchi， A. Fedorov， P. Konstantinov
CAUSES OF GREENLAND TEMPERATURE VARIABILITY OVER THE PAST 4000
YEARS: IMPLICATIONS FOR NORTH HEMISPHERIC TEMPERATURE CHANGE
T. Kobashi， K. Kawamura， K. Goto-Azuma， J. E. Box， C.-C. Gao，T. Nakaegawa

THE INTIERNATIONAL STUDY OF ARCTIC CHANGE: PROVIDING TIMELY,RELEVANT AND ACCESSIBLE SCIENTIFIC INFORMATION FOR RESPONDING
TO ARCTIC CHANGE
Peter Schlosser, Maribeth Murray, Lize-Marié van der Watt

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Poster Session
January 15, 2013 (Tuesday)
Core time 13:30-14:45 at Conference room 3Page
G1 (P1-P10)
G1-P1

Atmospheric science I
AEROSOL CHARACTERISTICS OVER NORWEGIAN ARCTIC: RESULTS FROMINDIAN SCIENTIFIC EXPEDITIONS
M. M. Gogoi, S. S. Babu, K. K. Moorthy，J. P. Chaubey，V. S. Nair，M. R. Manoj,
S. K. Kompalli，N. B. Lakshmi, R. C. Thakur，T. Meloth, S. Rajan
G1-P2
FLUCTUATION OF POLAR NIGHT JET WITH PROPAGATION OF THE AO FROMTHE STRATOSPHERE TO THE TROPOSPHERE
S. Kobayashi， H. L. Tanaka
G1-P3
COMBINED MEASUREMENTS OF GRAVITY WAVES WITH AN AIRGLOWIMAGER AND ALOMAR LIDARS IN NORWAY
S. Suzuki， F.-J. Luebken， G. Baumgarten， N. Kaifler， R. Eixmann，
B. P. Williams， T. Nakamura
G1-P4
VARIATIONS OF THE POLAR LOWER THERMOSPHERE, MESOSPHERE, AND
IONOSPHERE DUE TO A SSW ~A CASE STUDY OF THE JANUARY 2012
EVENT~
S. Nozawa， T. Kawahara， T. Tsuda， T. Kawabata， N. Saito， S. Wada，
Y. Ogawa， M. Tsutsumi
G1-P5
SODIUMDENSITY
VARIATION
DURING
AURORALPARTICLE
PRECIPITATIONS
T. T. Tsuda， S. Nozawa， T. D. Kawahara， T. Kawabata， N. Saito， S. Wada，
S. Oyama， Y. Ogawa， S. Suzuki， T. Takahashi， T. Nakamura
G1-P6
CURRENT STATUS OF THE STEL OPTICAL OBSERVATIONS AT THE TROMSOEEISCAT RADAR SITE
S. Oyama， S. Nozawa， R. Fujii， K. Shiokawa， Y. Otsuka， T. Takahashi
G1-P7
GRAVITY WAVE ANALYSIS USING METEOR WIND RADARS IN ARCTICNORWAY
M. Tsutsumi， C. Hall
G1-P8
EISCAT-JAPAN COLLABORATIVE STUDIES DRIVED BY EISCAT/EISCAT_3D
RADARS
H. Miyaoka， S. Nozawa， Y. Ogawa， S. Oyama， R. Fujii， C. Heinselman
G1-P9
THE POLARIZATION OF HIGHER HARMONIC AURORAL RADIO EMISSIONS
Y. Sato， T. Ono， N. Sato， Y. Ogawa， H. Yamagishi， A. Kadokura
G1-P10
CURRENT STATUS OF UPPER ATMOSPHERE PHYSICS OBSERVATION IN
ICELAND IN 2012
A. Kadokura， N. Sato， H. Yamagishi， Y. Tanaka， Y. Sato， T. Koshida，
M. Taguchi， T. Ono， T. Motoba， K. Hosokawa， Gunnlaugur Bjornsson(G5) Terrestrial ecosystem
G5-P1
ECOHYDROLOGY OF INTERIOR ALASKA BOREAL FOREST SYSTEMS
J. M. Cable， W. R. Bolton (CANCELLED)
G5-P2
SOIL CARBON FLUX IN BLACK SPRUCE FOREST AFTER FOREST FIRE,
INTERIOR ALASKA
Y. Kim， Y. Kodama， H. Harazono， H. Iwata
G5-P3
CRYOSPHERICAL COHESIVE REGIONS AS TERRESTRIAL RESEARCH IN
ALASKA FOR A COLLABORATIVE FRAMEWORK BETWEEN JAMSTEC AND
IARC
K. Sugiura， R. Suzuki， K. Saito， A. Ito， Y. Kim， H. Park， J. Cherry，
J. Walsh， J. Cable， S. Nagai， T. Nakai
G5-P4
THE JAMSTEC-IARC SUPERSITE ENHANCES UNDERSTANDING OF THE
ARCTIC CLIMATE SYSTEM - BIOGEOCHEMICAL OBSERVATIONS R. Suzuki， Y. Kim， S. Nagai， H. Kobayashi， T. Nakai， A. Ito
G5-P5
THE JAMSTEC-IARC SUPERSITE ENHANCES UNDERSTANDING OF THE
ARCTIC CLIMATE SYSTEM -HYDRO-METEOROLOGICAL OBSERVATIONST. Nakai， R.C. Busey， K. Sugiura， K. Saito， H. Park

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G5-P6ENVIRONMENTAL QUALITY MONITORING OF BIODIVERSITY WITHINCRYOLITHOZONE OF THE SAKHA REPUBLIC (YAKUTIA) IN THE CONDITIONSOF ECONOMIC USE AND GLOBAL CLIMATE CHANGE
N. G. Solomonov， I. M. Okhlopkov， S. Tatsuzawa
G5-P7
PHOTOSYNTHESIS OF LARIX LARICINA IN NORTHERN CANADA PERMAFROST
AREA
A. Maksimov， T. Maximov， A. Kononov
G5-P8
METHANE AND NITROUS OXIDE EXCHANGES BY DROPPINGS OF SVALBARD
REINDEER ORIGINATED FROM WINTER FOOD
K. Hayashi， W.A. Kishimoto-Mo， T. Motohka， M. Uchida， T. Nakatsubo
G5-P9
CHEMICAL CHANGES AND FUNGAL COLONIZATION OF SALIX ARCTICA
LEAF AND STEM LITTER ON DEGLACIATED MORAINES IN HIGH-ARCTICCANADA
T. Osono， D. Hirose， M. Uchida， H. Kanda
G5-P10
THE RELATIONSHIP BETWEEN PLANT AND SOIL BACTERIAL COMMUNITY IN
TUNDRA SOIL, ALASKA
H. Kim， J. Y. Jung， H. Lee， E. Yergeau， S. J. Nam， M. C. Kim， E. J. Lee，J. Chun， Y. K. Lee
G5-P11PERMAFROST DEPTH, FOREST FLOOR, AND FOREST BIOMASSACCUMULATION OF UPLAND BLACK SPRUCE STANDS IN INTERIOR ALASKA
Y. Matsuura， T. Morishita，K. Noguchi
G5-P12ESTIMATION OF C LOSS BY FIRE IN A BURNED BLACK SPRUCE FOREST IN
INTERIOR ALASKA USING RADIOCARBON.
M. Kondo， M. Uchida， Y. Shibata， H. Iwata， Y. Harazono
G5-P13RESPONSE OF ECOSYSTEM CARBON CYCLE TO CLIMATE CHANGE IN A
GLACIER FORELAND OF THE HIGH ARCTIC
M. Uchida， H. Muraoka， T. Nakatsubo(S5) GRENE Arctic project
S5-P1
MODEL RESOLUTION COMPARISON FOR METHANE SIMULATION IN THE
ARCTIC REGION
K. Ishijima， P. K. Patra， A. Ghosh， S. Morimoto， T. Machida，
M. Sasakawa， Y. Tojima， A. Ito, S. Aoki， T. Nakazawa
S5-P2
GLOBAL METHANE SIMULATION FOR THE PERIOD 1910-2010 USINGATMOSPHERIC GENERAL CIRCULATION MODEL BASED CHEMISTRY
TRANSPORT MODEL
A. Ghosh， P. K. Patra， K. Ishijima， S. Morimoto， K. Kawamura，
S. Aoki， T. Nakazawa， A. Ito
S5-P3
OCEANIC AND TERRESTRIAL BIOSPHERIC CO2 UPTAKE ESTIMATED FROMATMOSPHERIC POTENTIAL OXYGEN OBSERVED AT NY-ALESUND,SVALBARD AND SYOWA, ANTARCTICA
S. Ishidoya， S. Morimoto， S. Aoki， S. Taguchi， D. Goto， S. Murayama，T. Nakazawa
S5-P4
CONSTRUCTING ARCTIC CO2 DATA ASSIMILATION SYSTEM USING ONLINE
TRANSPORT MODEL AND LETKF
T. Maki， K. Miyazaki， Y. Sawa， H. Matsueda， T. Machida， T. Iwasaki
S5-P5
TIME SERIES OF TROPOSPHERIC N2O ISOTOPOMER RATIOS OVER WESTERNSIBERIA
S. Toyoda， N. Kuroki， N. Yoshida， K. Ishijima， Y. Tohjima， T. Machida
S5-P6
ANALYSIS OF INTER-ANNUAL VARIATIONS IN SEASONAL CYCLE OF APO AT
CAPE OCHI-ISHI
Y. Tohjima， H. Yamagishi， H. Mukai， T. Machida， C. Minejima
S5-P7
HIGH PRECISION CONTINUOUS MEASUREMENT SYSTEM FOR THE
ATMOSPHERIC O2/N2 RATIO AT NY-ALESUND, SVALBARD
D. Goto， S. Morimoto， S. Ishidoya， S. Aoki， T. Nakazawa
S5-P8
APPLICATION OF RADON-222 AS A TRACER FOR CHARACTERIZING FETCHREGIONS AND EVALUATING A GLOBAL 3D MODEL
C. Zhu， H. I. Yoshikawa， H. Matsueda， Y. Sawa， Y. Niwa， A. Wada，
H. Tanimoto
S5-P9
RECONSTRUCTION OF PAST VARIATIONS OF THE CARBON AND HYDROGEN
ISOTOPIC RATIOS IN ATMOSPHERIC METHANE FROM ITS VERTICAL
DISTRIBUTION OBSERVED IN NGRIP FIRN
S. Sugawara， T. Umezawa， K. Kawamura， S. Morimoto， S. Aoki，T. Nakazawa

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S5-P11

S5-P12
S5-P13
S5-P14S5-P15

S5-P16
S5-P17

S5-P18
S5-P19
S5-P20

S5-P21
S5-P22OBSERVATIONS OF ATMOSPHERIC GREENHOUSE GASES FROM A TOWER
NETWORK AND AIRCRAFT OVER SIBERIA
T. Machida， M. Sasakawa， Y. Sawa， H. Matsueda， S. Morimoto，
S. Murayama， Y. Niwa， K. Tsuboi， S. Aoki
GOALS AND ACTIVITIES OF THE TERRESTRIAL MODELING GROUP OF“GRENE ARCTIC CLIMATE CHANGE RESEARCH PROJECT”
K. Saito， T. Yamazaki， T. Ise， T. Hajima， M. Hosaka，A. Ito，
M. Niwano， R. O'ishi， H. Park，T. Sueyoshi， S. Yamaguchi
ARCTIC DATA ARCHIVE SYSTEM (ADS)
H. Yabuki， H. Kawamoto
RECENT GLACIER CHANGES IN SUNTAR-KHAYATA REGION, EASTERNSIBERIA.
H. Yabuki
CRYOSPHERIC STUDY IN THE GRENE-ARCTIC PROJECT: PLAN AND REPORTFROM RESEARCH IN 2012
H. Enomoto
OVERVIEW OF REGIONAL AND INTERANNUAL VARIATIONS OF SNOW AND
SURFACE CONDITIONS AT GRENE ARCTIC OBSERVATION SITES DERIVED BYSATELLITE MICROWAVE DATA
N. Alimasi， H. Enomoto， S. Takahashi
JAPANESE FIELD ACTIVITIES IN THE GREENLAND ICE SHEET MONITORINGNETWORK (GLISN)
G. Toyokuni， M. Kanao， Y. Tono， T. Himeno， S. Tsuboi
GLACIOLOGICAL OBSERVATIONS IN SUNTAR-KHAYATA RANGE, EASTERNSIBERIA, 2012
T. Shirakawa， T. Kadota， R. Kusaka， S. Tanaka， M. Miyairi， S. Takahashi，
H. Enomoto， T. Ohata， H. Yabuki， K. Konya， N. Takeuchi， A. Fedorov，
P. Konstantinov
IS WARMING ARCTIC CAUSING COLDER WINTERS IN SIBERIA?
V. Alexeev， Y. Tachibana， J. Cohen， I. Ezau
INFLUENCES OF THE SEA ICE CONCENTRATION AND SEA SURFACETEMPERATURE TO THE ATMOSPHERE
K. Terasaki， H. L. Tanaka
GREENLAND SST CHANGE AND ACCOMPANYING CHANGES IN THE
NORTHERN HEMISPHERIC CLIMATE AND PREDICTABILITY OF THE NORTHATLANTIC OSCILLATION
M. Nakamura
DEVELOPMENT OF A LOWER TROPHIC LEVEL ECOSYSTEM MODEL FOR
ARCTIC OCEAN
T. Terui， E. Watanabe， MJ. Kishi
SEA-ICE THICKNESS CHARACTERISTICS REVEALED BY OBSERVATIONS IN
THE CANADA BASIN
J. Ono， K. Tateyama， D. Hirano， A.Orlich

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January 16, 2013 (Wednesday)
Core time 13:30-14:45 at Conference room 3
Page(G3) Hydrology, permafrost and snow cover
G3-P1
MRI LAND SURFACE SCHEME HAL
M. Hosaka
G3-P2
RECENT VARIABILITY OF AIR TEMPERATURE IN NORTH-EAST EURASIA ANDITS EFFECT ON PERMAFROST LANDSCAPES
A. Fedorov， P. Konstantinov， R. Ivanova， Y. Iijima， H.Park
G3-P3
THE USE OF SITES WITH A THICK GRID OF THAW TUBES TO OBSERVATION
THE DEPTH OF SEASONAL THAWING IN CENTRAL YAKUTIA
P.Ya.Konstantinov， A.N.Fedorov， I.S.Ugarov， R.N.Argunov， Y.Iijima
G3-P4
PERMAFROST DEGRADATION AND FLOOD OCCURRENCE IN THE FAR NORTH
OF SIBERIA
T. Sakai， T. Hiyama， J. Fujiwara， S. Gotovtsev， L. Gagarin， Y. Yamaguchi
G3-P5
IMPROVED ALGORITHM FOR MODELLING OF HEAT DYNAMICS IN FROZENSOILS
O. Semenova， Y. Vinogradov， L. Lebedeva
G3-P6
MODELLING OF ACTIVE LAYER DEPTH DYNAMICS AND RUNOFFFORMATION AT SMALL WATERSHED ENTIRELY COVERED BY BARE ROCKS
L. Lebedeva， O. Semenova， T. Vinogradova， E. Boyarintsev
G3-P7
GEOCRYOLOGICAL CHARACTERISTICS OF THE SEDIMENT NEAR THE
PERMAFROST TABLE IN THE DOWNSTREAM FLOOD PLANE OF THE
INDIGIRGA RIVER, RUSSIA
G. Iwahana， S. Takano， S. Tei， R. Shingubara， T. C. Maximov， A. Sugimoto
G3-P8
MONITERING OF SURFACE AND SUBSURFACE CONDITIONS IN PERMAFROSTAREA AFTER WILDFIRE, ALASKA
K. Harada， K. Narita， K. Saito， Y. Sawada， G. Iwahana， M. Fukuda
G3-P9
THE INFLUENCE OF GROUNDWATER FLOW ON TALIK DEVELOPMENT IN A
SMALL PERMAFROST FEN
Y. Sjoberg， A. Frampton， S. Lyon， B. Sannel (CANCELLED)
G3-P10AGE ESTIMATION OF SUPRA-PERMAFROST AND INTRA-PERMAFROSTGROUNDWATER IN YAKUTSK REGION, EASTERN SIBERIA
T. Hiyama， K.Asai， L. Gagarin， A. Kolesnikov
G3-P11WESTERN AND CENTRAL SIBERIA HYDROLOGICAL CYCLE FROM SATELLITE
AND IN SITU OBSERVATIONS
E. A. Zakharova， A. V. Kouraev， S. N. Kirpotin，I. Krylenko(G6) Marine ecosystem
G6-P1
PHOTOPROTECTIVE RESPONSES OF ICE ALGAE AFTER LIGHT EXPOSURE IN
SAROMA-KO LAGOON, HOKKAIDO, JAPANT. Katayama， K. Takimoto， S. Motokawa， M. Obata， S. Taguchi
G6-P2
PHYSYIOLOGICAL AND MORPHOMETRICAL RESPONSES OF SUBARCTIC
COCCOLITHOPHORE, EMILIANIA HUXLEYI, TO TEMPERATURE
K. Saruwatari， M. Satoh， N. Harada， I. Suzuki， Y. Shiraiwa
G6-P3
ANALYSIS OF THE CHARACTERISTICS IN THE COCCOLITHOPHORE,
EMILIANIA HUXLEYI ISOLATED FROM ARCTIC SEA
F. Itoh， M. Satoh， N. Harada， I. Suzuki， Y. Shiraiwa
G6-P4
HORIZONTAL DISTRIBUTION OF BACTERIAL ASSEMBLAGES ON SURFACESEDIMENTS IN THE ARCTIC OCEAN
D. Han， S. Il Nam， Y. K. Lee， H. G. Hur
G6-P5
SPATIAL DISTRIBUTIONS OF BACTERIO- AND VIRIOPLANKTON IN THE
CHUKCHI SEA DURING SUMMER 2012
C.Y. Hwang， Y.Y. Yang， Y.K. Lee， S.-H. Kang
G6-P6
MACROMOLECULAR COMPOSITIONS OF PHYTOPLANKTON IN THE
NORTHERN CHUKCHI SEA
J. H. Lee， H. T. Joo， J. W. Park， J. J. Kang， S. H. Lee
G6-P7
DISTRIBUTION OF PHYTOPLANKTON COMMUNITIES IN THE BERING,CHUKCHI SEA AND CANADIAN BASIN DURING SUMMER
H. M. Joo， D. B. Lee， K. H. Chung， S. H. Lee， J. H. Lee， S. H. Kang
G6-P8
DISTRIBUTION OF MESOZOOPLANKTON RELATED TO THE ENVIRONMENTAL
FACTORS IN THE CHUKCHI SEA, 2011
D. B. Lee， H. M. Joo， H. K. Ha， E. J. Yang， K. H. Chung， S. H. Kang

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G6-P9SEASONAL CHANGES IN MESOZOOPLANKTON SWIMMERS COLLECTED BY
SEDIMENT TRAP MOORED IN THE WESTERN ARCTIC OCEAN
K. Matsuno， A. Yamaguchi， I. Imai， J. Onodera，S. Chiba， N. Harada(S2) Changes in water and carbon cycles of terrestrial ecosystem on permafrost in a warming Arctic
S2-P1
SOIL MOISTURE AND PERMAFROST CONDITIONS AT NEWLY ESTABLISHEDYAKUTSK-VILYUY TRANSECT
Y. Iijima， A. N. Fedorov， P. Y. Konstantinov， H. Park
S2-P2
ECOHYDROLOGY IN ALASKA'S BOREAL FOREST: INTERPRETING
MEASUREMENTS OF WATER VAPOR ISOTOPES FROM AIRCRAFT AND
SATELLITE SENSORS
J. Cherry， J. Cable， J. Worden， R. Herman， J. Welker
S2-P3
RECONSTRUCTION OF PAST 100 YEARS SOIL MOISTURE IN EASTERN SIBERIABY USING DELTA-13C OF LARCH TREE RINGS
S. Tei， A. Sugimoto， H. Yonenobu， T. Yamazaki， T. Maximov
S2-P4
INVESTIGATION OF ENERGY BALANCE ABOVE A LARCH FOREST IN
CENTRAL YAKUTIA
R. E. Petrov， A. V. Kononov， T. C. Maximov
S2-P5
SOIL WATER CHANGE IN EASTERN SIBERIAN TAIGA FORESTS SIMULATEDBY A ONE-DIMENSIONAL LAND-SURFACE MODEL
T. Yamazaki， S. Tei， A. Sugimoto， T. Ohta
S2-P6
FINE ROOT BIOMASS OF BLACK SPRUCE AT STANDS WITH DIFFERENT
DEPTHS OF PERMAFROST TABLE
K. Noguchi， Y. Matsuura， S. Sparrow， L. Hinzman
S2-P7
ENERGY AND CARBON EXCHANGES OVER THE LARCH FORESTS ON THE
PERMAFROST IN MONGOLIA
S. Miyazaki， M. Ishikawa， N. Baatarbileg， S. Damdinsuren， Y. Jambaljav
S2-P8
FEATURES OF SOIL CO2 EFFLUX IN TAIGA LARCH FORESTS OF CENTRALAND SOUTH-EASTERN YAKUTIA
A. V. Kononov， A. P. Maksimov，R. E. Petrov，T. C. Maximov
S2-P9
PERMAFROST CARBON AND CLIMATE FEEDBACKS ENHANCE ARCTICECOHYDROLOGICAL PROCESSES
H. Park， J. Walsh
S2-P10APPLICATION OF STABLE ISOTOPE RATIOS OF C AND N TO CARBONASSIMILATION AND NITROGEN UTILIZATION OF LARCH IN ARCTICECOSYSTEM OF EASTERN SIBERIA
M. Liang， S. Tei， T. C. Maximov， S. Kiyashko， T. A. Velivetskaya，
A. V. Ignatiev， A. Sugimoto
S2-P11
THE EFFECT OF THE FEEDBACK CYCLE BETWEEN THE SOIL ORGANICCARBON AND THE SOIL HYDROLOGIC AND THERMAL DYNAMICS
K. Mori， T. Ise， M. Kondo， Y. Kim， H. Enomoto， M. Uchida
S2-P12
DYNAMICS AND LARCH UPTAKE OF NITROGEN IN THE NORTH EASTERNSIBERIA TAIGA FOREST
A. Popova， N. Tokuchi， N. Ohte， T. Maximov， A. Sugimoto
S2-P13
DEVELOPING A METHANE EMISSION MODEL FOR SIBERIAN RIVER
FLOODPLAINSY. Mi， J. van Huissteden
S2-P14METHANE AND ORGANIC MATTER IN PERMAFROST OBSERVED AT
CHOKURDAKH (EASTERN SIBERIA)
I. Bragin， M. Nakamura， S. Takano， G. Iwahana， R. Shingubara， R. Petrov，T. Maximov，T. Velivetskaya， A. Ignatiev， S. Kiyashko， A. Sugimoto
S2-P15CH4 EMISSION FROM A TAIGA-TUNDRA ECOTONE OF EASTERN SIBERIA:PROCESS STUDY BY STABLE ISOTOPES
R. Shingubara， A. Sugimoto， T. C. Maximov
S2-P16
INCREASED GREENHOUSE GAS EMISSION FROM THAW PONDS IN SIBERIANARCTIC TUNDRA ON CONTINUOUS PERMAFROST.
A. Gallagher， A. Budischev， B. Li， J. van Huissteden， M.M.P.D.Heijmans，
A. J. Dolman

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179

180
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183

184
185

(S3) Changes in the Greenland ice sheet in the context of interactions with the atmosphere and the ocean
S3-P1
INTENSIVE OBSERVATIONS OF METEOROLOGICAL AND SNOW-PHYSICAL
PARAMETERS AT SITE SIGMA-A IN NORTHWESTERN GREENLAND IN
SUMMER 2012
T. Aoki， S. Matoba， S. Yamaguchi， T. Tanikawa， W. Niwano， T. Yamasaki，
K. Kuchiki， H. Motoyama， M. Hori
S3-P2
MELTING RECORD IN NORTHWESTERN GREENLAND ICE SHEETS. Matoba， S. Yamaguchi， T. Yamasaki， T. Tanigawa， T. Aoki， M. Niwano，
H. Motoyama
S3-P3
MEASUREMENT OF SPECIFIC SURFACE AREA OF SNOW COVER IN
GREENLAND
S. Yamaguchi， S. Matoba， T. Aoki， M. Niwano， T. Tanikawa， T. Yamasaki，
A. Hachikubo
S3-P4
NUMERICAL SIMULATION OF SUMMER SNOWMELT AT SITE SIGMA-ANORTHWESTERN GREENLAND DURING 2012 INTENSIVE OBSERVATIONS
M. Niwano， T. Aoki， S. Yamaguchi， S. Matoba， T. Tanikawa， T. Yamasaki，
K. Kuchiki， H. Motoyama
S3-P5
MONITORING OF THE DARK REGION ON GREENLAND BY AQUA/MODIS
DURING THE MELTING SEASON 2002 - 2012
T. Tanikawa， T. Aoki， M. Hori
S3-P6
MASS CONCENTRATION OF SNOW IMPURITIES AND SNOW GRAIN SIZE ONNORTHWESTERN GREENLAND ICE SHEET: COMPARISON BETWEENRETRIEVAL FROM MODIS AND IN-SITU MEASUREMENT
K. Kuchiki， T. Aoki， H. Motoyoshi， S. Matoba， S. Yamaguchi，T. Tanikawa，
M. Niwano， R. Shimada， T. Yamasaki
S3-P7
ICE FRONT VARIATIONS AND VELOCITY OF OUTLET GLACIERSTERMINATING IN INGLEFIELD FJORD, THE NORTHWEST GREENLAND
D. Sakakibara， S. Sugiyama
S3-P8
THINNING OF AN ICE CAP AT THE COASTAL MARGIN OF NORTHWESTERNGREENLAND
S. Matsuno， S. Sugiyama， D. Sakakibara， S. Yamaguchi， S. Matoba，
T. Sawagaki
S3-P9
MICROBIAL COMPOSITION CHANGES IN CRYOCONITE FORMATION PROCESSIN NORTHWESTERN GREENLAND
J. Uetake， N. Takeuchi， N, Nagatsuka， H. Motoyama， T. Aoki
EFFECT OF MICROORGANISM ON GREENLAND ICE SHEET SURFACE
S3-P10TEMPERATURE CHANGE
R. Shimada， N. Takeuchi， T. Aoki

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191

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January 17, 2013 (Thursday)
Core time 12:55-14:10 at Conference room 3Page
G1 (P11-P18) Atmospheric science II
G1-P11
IMPACT OF NICAM-LETKF ON THE ARCTIC
K. Kondo， H. L. Tanaka， M. SatohG1-P12DECADAL VARIABILITY AND A RECENT AMPLIFICATION OF THE SUMMERBEAUFORT HIGH: IMPLICATIONS FOR SEA-ICE, UPWELLING AND POLYNYASIN THE WESTERN ARCTIC OCEAN
G. W. K. Moore， R. S. Pickart
G1-P13
RECENT LINKAGE BETWEEN SPRING SNOW COVER AND SUMMER ARCTICSEA ICE EXTENTS. Matsumura， X. Zhang
G1-P14
CHANGES IN THE LENA RIVER DISCHARGE AND NET PRECIPITATION OVER
THE BASIN DURING 2005-2008
K. Oshima， Y. Iijima， M. E. Hori， J. Inoue， T. Hiyama
G1-P15
ANNUAL CLOUD VARIATION OBSERVED AT NY-ALESUND FROM 2005 TO
2008
K. Nishinaka， M. KUJI， M. Yabuki， M. Shiobara
G1-P16
THE STRUCTURE OF THE ARCTIC CYCLONE IN SUMMER ANALYZED BY THE
JRA-25/JCDAS REANALYSIS DATA
A. Yamagami， H. L. Tanaka
G1-P17
MICROPHYISICAL PROPERTIES OF BOUNDARY LAYER MIXED-PHASE CLOUDOBSERVEDIN
NY-ALESUND,SVALBARD(OBSERVED
CLOUDMICRO-PHYSICS AND CALCULATED OPTICAL PROPERTIES)
A. Uchiyama， M. Shiobara， A. Yamazaki， H. Kobayashi
G1-P18DIAGNOSTIC ANALYSIS OF THE DECADAL VARIABILITY OF THE ARCTICOSCILLATION USING THE AOI EQUATION
M. Kino， H. L. Tanaka(G2) Ocean and sea ice
G2-P1
ARCTIC SEA ICE VARIABILITY DERIVED FROM AN EXPANDED SEA ICEDATABASE, 1850-2012
J. E. Walsh， W. L. Chapman， F. Fetterer
G2-P2
NUMERICAL SIMULATION OF THE ARCTIC SEA ICE VARIABILITY
H. J. Lee， M. O. Kwon， Y. K. Seo， D. C. Park
G2-P3
THE ENERGY BUDGET OF ARCTIC FIRST-YEAR SEA ICE THROUGH THE MELTSEASONS. Hudson， M. A. Granskog， D. Divine， C. Polashenski， J. Ehn，C. Pedersen， A. Sundfjord， A. Renner， S. Gerland
G2-P4
MOORING MEASUREMENT OF SEA-ICE THICKNESS IN THE CHUKCHI SEA OFFBARROW ALASKA
D. Simizu， Y. Fukamachi， K. I. Ohshima， K. Iwamoto， C. Petrich，A. Mahoney， H. Eicken
G2-P5
INFLUENCE OF OCEAN THERMAL CONDITION ON THE WINTERTIME SEA ICE
EXTENT VARIABILITY IN THE BARENTS SEA
T. Nakanowatari， J. Inoue
G2-P6
FORMATION PROCESSES OF SEA ICE BAND FORMED BY CONVERGENCE OF
SEA ICE MOTION IN THE PACIFIC SECTOR OF THE ARCTIC OCEAN-AVAILABILITY OF ARCTIC SEA ROUTESE. Yoshizawa， K. Shimada
G2-P7
EVIDENCE OF SUBMARINE MASS WASTING EVENT IN MOLLOY HOLE, FRAMSTRAIT USING MULTIBEAM BACKSCATTER
F. Freire， R. Gyllencreutz， M. Jakobsson
G2-P8
DISTRIBUTION OF CaCO3 UNDERSATURATED WATERS IN THE ARCTICOCEAN, RECONSTRUCTED FROM HISTRICAL DATA
M. Yamamoto-Kawai
G2-P9
REDUCED SPACE 4DVAR TECHNIQUE
AS A POTENTIAL TOOL FOR
REANALYSIS AND OPERATIONAL HIND-CAST IN THE ARCTIC OCEAN
G. Panteleev， M. Yarenchuk， O.Francis
G2-P10 SEDIMENTARY ORGANIC MATTER AND CARBONATE VARIATIONS IN THE
CHUKCHI BORDERLAND IN ASSOCIATION WITH ICE SHEET AND
OCEAN-ATMOSPHERE DYNAMICS OVER THE LAST 155 KYR
S. F. Rella， M. Uchida

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199
200
201
202

203

204
205
206

207

208
209

210
211
212
213

(G4) Ice sheets, glaciers and ice cores
G4-P1
CHEMICAL COMPOSITIONS OF SOLUBLE AEROSOLS AROUND THE
TERMINATION 1 IN THE NEEM ICE CORE
I. Oyabu， Y. Iizuka， T. Karlin， M. Fukui， T. Hondoh， M. Hansson
G4-P2
EARLY TWENTIETH CENTYRY WARMING VEIWED FROM ARCTIC ICE CORES
K. Goto-Azuma
G4-P3
CONCENTRATION OF TRACE INORGANIC SPECIES IN SURFACE SNOW AT
NEEM, GREENLAND
M. Hirabayashi， K.Goto-Azuma， H. Motoyama， D. Dahl-Jensen，
J. P. Steffensen
G4-P4
THE VARIABILITY MECHANISM OF PRECIPITATION AMOUNT IN CENTRALALASKA
A. Tsushima， S. Matoba， T. Shiraiwa
G4-P5
50-YEARS GLACIAL ENVIRONMENTAL CHANGE IN BENNETT ISLAND,SIBERIAN ARCTIC
K. Konya， T. Kadota， H. Yabuki， T. Ohata
G4-P6
DNA ANALYSIS FOR SECTION IDENTIFICATION OF A PINE POLLEN GRAINFROM THE BELUKHA GLACIER, ALTAI MOUNTAINS, RUSSIA
F. Nakazawa， J. Uetake， Y. Suyama， R. Kaneko， N. Takeuchi， K. Fujita，
H. Motoyama， S. Imura， H. Kanda(G7) Interdisciplinary modeling studies
G7-P1
NUMERICAL STUDY OF AEROSOL EFFECTS IN ARCTIC MIXED-PHASE
CLOUDS VIA THE LIQUID PHASE
G. de Boer， T. Hashino， G. J. Tripoli， E. W. Eloranta
G7-P2
BJERKNES COMPENSATION AND ITS ROLE IN THE ARCTIC
S. Outten， I. Esau
G7-P3
THE ROLE OF ATMOSPHERIC CIRCULATION FOR SEA ICE ON THE ARCTIC BY
APPLYING THE CMIP3 MODEL
H. Hirano， M. Ogi， T. Yoshihiro
G7-P4
INFLUENCE OF RETREATING SEA ICE ON CLOUD COVER OVER THE ARCTICOCEAN DURING RECENT GLOBAL WARMING PERIOD
M. Abe， T. Nozawa， T. Ogura， K. Takata
G7-P5
MODELING HIGH WIND EVENTS IN A REGIONAL ARCTIC SYSTEM MODEL
J. Cassano， A. DuVivier， M. Hughes
G7-P6
DEVELOPMENT OF AN ENSEMBLE DATA ASSIMILATION SYSTEM WITH WRF
FOR THE LAND-ATMOSPHERE INTERACTION IN ARCTIC
K. Suzuki， M. Zupanski
G7-P7
LARGE SCALE VARIATIONS OF THE ENERGY-WATER BALANCE AT THE
LAND SURFACE USING A WETNESS INDEXK. Takata， J. Xu， M. Hara， T. Nozawa(S1) Polar (Arctic) amplification in global warming
S1-P1
SEA ICE VARIABILITY IN THE BARENTS SEA BRINGS ARCTIC WARMTH AND
CONTINENTAL COLD
J. Inoue， M. E. Hori， K. Takaya
S1-P2
CONTRIBUTION OF FROZEN HILLOCKS TO METHANE EMISSION FROM WESTSIBERIAN TUNDRA MIRES
M. V. Glagolev， A. F. Sabrekov， I. E. Kleptsova， S. S. Maksyutov，
P. A. Barsukov， V. N. Bashkin
S1-P3
THE RELATIONSHIP BETWEEN ARCTIC OSCILLATION AND ARCTICWARMING IN RECENT DECADESY. Nagato， H. L. Tanaka
S1-P4
ABRUPT CLIMATE CHANGES AND EMERGING ICE-OCEAN PROCESSES IN THE
PACIFIC ARCTIC REGION AND THE BERING SEA
J. Wang， M. Ikeda(S4) International cooperation on Arctic observation and research
S4-P1
USING BIG DATA ANALYTICS, SCENARIOS DEVELOPMENT, AND GAMETHEORY TO MONITOR, UNDERSTAND AND ADAPT TO CLIMATE CHANGE IN
THE CIRCUMPOLAR ARCTIC
M.A.K. Muir， M. E. Goodsite(S6) Monitoring of the Arctic environment
S6-P1
RADIOCESIUM IN THE SEDIMENTS OF THE RUSSIAN ARCTIC SEAS
D. Alexeev， V. Galtsova

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217
218
219

220
221
222
223
224
225
226

227
228

229
230

231

232

S6-P2

S6-P3

KOLYMA WATER-BALANCE STATION - UNIQUE RESEARCH STATION IN THE
ZONE OF CONTINUOUS PERMAFROST: HALF CENTURY HISTORY AND
FUTURE PERSPECTIVES
L. Lebedeva， O. Semenova， E. Boyarintsev
VISIBLE REMOTE SENSING INFORMATION FOR SNOW MONITORING
I. Appel

233

234

January 17, 2013 (Thursday)
17:10- Closing Session
Reports by the conveners of Special Sessions
Discussion
Closing speech Atsuko Sugimoto (Co-chair of ISAR-3 Organizing Committee)

Added
G7-P8

TOWARD HIERARCHICAL MODELING AND PREDICTION OF THE ARCTIC
CLIMATE SYSTEM
Wieslaw Maslowski, Jaclyn Clement Kinney, Andrew Roberts, Anthony Craig,
Robert Osinski, John J. Cassano, William J. Gutowski, Bart Nijssen, Dennis P.
Lettenmaier, William H. Lipscomb, Slawek M. Tulaczyk, Xubin Zeng

xx

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Banquet location
Hotel Nikko Tokyo 1st floor "Appolon"   

Banquet location (In Japanese)
Hotel Nikko Tokyo 1st floor "Appolon"
ACCESS MAP

大宮駅

Omiya St.

JR 埼京線は大崎駅でりんかい線に乗り入れ

By Taxi

タクシーをご利用の場合
JR新橋駅から...................................................... 約15分
JR田町駅から（レインボーブリッジ経由） .......... 約12分
JR品川駅から ..................................................... 約20分
JR東京駅から ..................................................... 約20分
新木場駅から...................................................... 約10分
六本木駅から...................................................... 約30分
銀座駅から........................................................... 約20分
東京ディズニーリゾート（JR舞浜駅）から（高速道路利用）..............................................約20分
羽田空港から（高速道路利用）..............................................約15分

From JR Shimbashi St. ..................................................... 15 min.

J

JR Y R 山
am 手
an 線
ote
Lin
e

大江戸線

池袋駅

Toei Oedo Line

From JR Tamachi St. ......................................................... 12 min.

Ikebukuro St.

From JR Shinagawa St. ................................................... 20 min.

新宿駅

From JR Tokyo St. .............................................................. 20 min.

Shinjuku St.

上野駅

Ueno St.

浅草駅

Asakusa St.

有楽町線

From Shin-kiba St. .............................................................. 10min.

Tokyo Metro
Yurakucho Line

From Roppongi St. ............................................................ 30 min.

渋谷駅

From Ginza St. ..................................................................... 20 min.

Shibuya St.

From Tokyo Disney Resort / JR Maihama St.

東京駅

Tokyo St.

銀座線

(of the Metropolitan Expressway) ............. 20 min.

Tokyo Metro Ginza Line

恵比寿駅

From Haneda Airport

有楽町駅

浜松町

Ebisu St.

(of the Metropolitan Expressway) ............ 15 min.

JR 京葉線

Yurakucho St.

Hamamatsucho St.

JR Keiyo Line

新橋駅

Shimbashi St.

成田国際空港から「臨海副都心行き」乗車 ............................ 約 75 分
羽田空港から
「臨海副都心行き」乗車 ............................ 約 20 分

From Narita International Airport

お台場レインボーバスをご利用の場合
品川駅東口〜ホテル日航東京................ 約 30 分

By Odaiba Rainbow Bus＊所要時間は交通状況により変わることがございます。

*The travel time will vary depending on traﬃc.

大崎駅

品川駅

Osaki St. Shinagawa St.

都営浅草線.................................................................. 75min.

Toei Asakusa Line

From Haneda Airport.................................................................. 20min.

大井町駅

Oimachi St.

JR 京浜東北線

JR Keihin-tohoku Line

Shinagawa St. East Exit -ゆり

Kawasaki St.

横浜駅

Toyosu St.

Shin-kiba St.
Daiba St.

東
京
モ
ノ
レ
ー
ル

りんかい線
東京テレポート駅

Haneda Airport
International Terminal St.

京急蒲田駅

keikyu-kamada St.

Rinkai Line

Tokyo Teleport st.

羽田空港国際線ターミナル駅

Yokohama St.

新木場駅

台場駅

e

川崎駅

Hotel Nikko Tokyo ....................... 30min.

豊洲駅

Yur かも
ika
mo め
me
Lin

天
王
洲
ア
イ
ル
駅

Tokyo Monorail

By Airport Limousine Bus
Tennozu Isle St.

リムジンバスをご利用の場合

羽田空港国内線ターミナル駅
Haneda Airport
Domestic Terminal St.

京浜急行空港線
Keikyu Kuko Line

京浜急行本線

Keikyu Honsen Line

羽田空港第 1 ビル駅

Haneda Airport Terminal 1

羽田空港第 2 ビル駅

Haneda Airport Terminal 2〒135-8625 東京都港区台場1-9-1 1-9-1, Daiba, Minato-ku, Tokyo 135-8625
Tel.03-5500-5500（代表） www.hnt.co.jp

新宿

Shinjuku St.

東京スカイツリー

上野Tokyo Sky Tree

お車をご利用の場合
首都高速 11 号台場線
台場ランプから .................................... 約 3 分
首都高速湾岸線
臨海副都心ランプから ..................... 約 3 分
首都高速湾岸線
有明ランプから .................................... 約 4 分
首都高速 10 号晴海線
有明ランプから .................................... 約 4 分

Ueno St.

東京ミッドタウン
Tokyo-Midtown

雷門

Kaminarimon

皇居

原宿

秋葉原

Imperial Palace

Akihabara St.

Harajuku St.

東京タワー

六本木

Tokyo-Tower

Roppongi St.

東京

大
江
戸
線

Shibuya St.

六本木ヒルズTokyo MetroYurakucho Line

汐留

Shiodome St.

Hamamatsucho St.

竹芝

Takeshiba St.

田町

日の出

Tamachi St.

月島eTsukishima St.

芝浦ふ頭

Shibaura-futō St.

京葉線

レインボーブリッジ大崎

Osaki St.

Rainbow Bridge

品川

新豊洲

市場前

Shinagawa St.

台場ランプ

Shin-toyosu St.

Shijo-mae St.

豊洲

Toyosu St.

Daiba Ramp

首都高速 10 号
晴海線

東
海
道
・
京
浜
東
北
線

賀線Line
ka
横須
kosu
o

JR Y

Metropolitan Expressway
Route No.10 Harumi Line

Tennozu-Isle St.

お台場海浜公園

台場e

品川シーサイド

東京テレポート

Rinkai Fukutoshin Ramp

Tokyo Teleport St.

JR
Ke Tokihin aid
-to o
ho
ku

Lin

Shinagawa Seaside St.

Palette Town

Bay Sho

Metropolitan Exp

Monor
ai

l

東
京
モ
ノ
レ
ー
ル

首
都
高
速
湾
岸
線

船の科学館

Fune-no-kagakukan St.

Aomi St.

国際展示場

Kokusai-tenjijō St.

りんかい線

有明

Airportto Haneda

Airpor
neda

至
羽
田
空
港

至
羽
田
空
港

東雲

Rinkai Line

新木場

Shin-kiba St.

Shinonome St.

Rinkai Line

Ariake St.

Shimbashi St. - Daiba St. ....... 15 min.
Toyosu St. - Daiba St. .............. 16 min.
*Directly Connected to Daiba St.
Osaki St. - Tokyo Teleport St. ...... 11 min.
Shin-kiba St. - Tokyo Teleport St. ... 7 min.
*A 10-minute walk from Tokyo Teleport St.
A free shuttle bus is also operated
from Tokyo Teleport St.

国際展示場正門

Kokusai-tenjijō-seimon St.

臨海副都心・台場地区周辺の交通図 Rinkai-fukutoshin Daiba Area Traﬀic Chart

東京ビッグサイト

台場入口
Daiba Ramp

Tokyo Big Sight

ゆ
り
か
も
め

台場出口
Daiba Ramp

レインボーブリッジ
一般道入口

水上バス

Water Bus St.

Lower Level Road : Rainbow Bridge

アクアシティお台場 デックス東京ビーチ
AQUA CiTY ODAIBA

テレコムセンター
Telecom Center St.

t

Tokyo

Expr

essw

首
都
高
速
1
号
線

ressway

ay Ro

ute N

o.1

re Route

青海

to Ha

Yurikamome Line

Ariake Ramp

臨海副都心ランプ

パレットタウン

litan

By Train

大江戸温泉物語

Oedo-Onsen Monogatari首都高速道路 Metropolitan Expressway
新交通ゆりかもめ Yurikamome Line
りんかい線 Rinkai Line

東京モノレール Tokyo Monorail
一般道 Trunk Road

ゆ
り
か
も
め

DECKS Tokyo Beach

台場 Daiba St.
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Abstract

KN–1

㻔

KN–2

㻕

KN–3

㻖

G1–O1㻗G1–O2㻘

G1–O3㻙

G1–O4㻚

G1–O5㻛G1–O6㻜

G1–O7

㻔㻓

G1–O8㻔㻔

G1–O9㻔㻕

G1–O10㻔㻖G1–O11㻔㻗

G1–O12㻔㻘G1–O13㻔㻙

G1–O14㻔㻚

S5–O1㻔㻛S5–O2㻔㻜

S5–O3㻕㻓

S5–O4㻕㻔

S5–O5㻕㻕㻪㻘㻐㻲㻔
G5–O1

CROSS-DISCIPLINARY RESEARCH COLLABORATION FOREARLY DETECTION OF BIOLOGICAL FEEDBACKS
Nobuko Saigusa1, Rikie Suzuki2, Tetsuya Hiyama3, Kentaro Hayashi41National Institute for Environmental Studies, Tsukuba, Japan
Japan Agency for Marine-Earth Science and Technology, Yokohama, Japan
3
Research Institute for Humanity and Nature, Kyoto, Japan
4
National Institute for Agro-Environmental Sciences, Tsukuba, Japan
E-mail: n.saigusa@nies.go.jp
2

To predict global climate change and its influence on ecosystems andhuman societies, reliable understanding of land surface - atmosphere interactions
is essential. We will report current status and issues of internationalcross-disciplinary research collaborations focusing on early detection of biologicalfeedbacks to climatic change. One of our urgent tasks is to develop monitoring
systems for the spatial distribution and temporal variation of fluxes of energy,
water, carbon and various biogenic trace gases at scales ranging from point tocontinental. Relevant programs and the potential of collaboration will be
introduced based on Asian regional activities in international projects such asiLEAPS*, FLUXNET**, and ILTER network***.
Positive biological feedbacks include higher temperatures bringing higher
emissions of GHGs (CO2 and CH4) and irreversible changes that may occur invulnerable ecosystems such as permafrost and peatlands. Negative feedbacks
include higher temperatures expanding the growth area of plants in arctic regions
and the rising atmospheric CO2 concentration enhancing the growth rate of plants
by a fertilization effect. To detect such biological feedbacks in regional andcontinental scales, cross-disciplinary research collaboration helps scientists
develop integrated long-term observation networks. In mid-latitudes, JapanFlux (asub-network in FLUXNET) and JaLTER (Japan national network in ILTER) havestarted working together by sharing sites, data, and observational skills toward
maintaining long-term comprehensive observation networks. The long-term
ground observations of phenology are also expanding using spectral radiometersand camera images for verification of satellite remote sensing.
Cross-disciplinary research collaboration at integrated observations helps
us develop comprehensive datasets, which accelerate the development andtesting of various process-based ecosystem models. Long-term ground-truth
datasets with appropriate spatial resolution will have high value for directcomparison with airborne and satellite remote sensing. The research communities
growing at integrated observation platforms will also contribute to educating thenext generation of scientists by bridging different disciplines.

_________________________________*iLEAPS: integrated Land Ecosystem - Atmosphere Process Study; the landatmosphere core project of the International Geosphere-Biosphere Programme(IGBP).
**FLUXNET: The worldwide network of monitoring sites for energy, water vapor,and CO2 fluxes over terrestrial ecosystems;. an iLEAPS recognized project.
***LTER network: International Long Term Ecological Research; an endorsed
network of the Global Land Project (GLP), a joint core Project of IGBP and theInternational Human Dimensions Programme (IHDP).

㻕㻖㻪㻘㻐㻲㻕

G5–O2

LONG TERM VARIABILITY OF CARBON IN PERMAFROSTDOMINATED ECOSYSTEMS
Maximov T.1,5, Dolman A.J.2, Huissteden J.2, Ohta T.3, Sugimoto A.4, Kononov A.1,5,
Maksimov A.1, Petrov E. 1,5, Terentyeva M. 1
1

Institute for Biological Problems of Cryolithozone SD RAS, Russia
Vrije Universiteit of Amsterdam, The Netherlands;
3
Nagoya University, Japan;
4
Hokkaido University, Japan
5
BEST Center of North Eastern Federal University, Russia
E-mail address of corresponding author: t.c.maximov@ibpc.ysn.ru
2This report is compiled on the results of multi-year investigations conductedwithin the frameworks of international scientific programs in cooperation with scientists
from Japan and European Union on the study of carbon and water cycles in permafrost
region, as well as execution of thematic plans of the IBPC SB RAS.
For the first time in the conditions of Eastern Siberia an attempt has been madeto ground the photosynthetic productivity of plants in terms of physiology, andquantitative parameters of the productive process were obtained. Original data on sinksource system of plants are stated at the levels of whole plant organism andcommunity. A number of specific results have been got: 1) conclusion was made abouthigh depositing role of the root system of high latitude plants; 2) micrometeorologicalestimates of carbon balance were done; 3) quantitative dependence of CO2
concentration on the season period, weather condition and forest fire intensity was
shown; 4) carbon parameters of forest and tundra ecosystems were investigated; 5)attention was drawn to short vegetative period of plant development  this feature
contributes to enrichment of the atmosphere of high latitudes by carbon dioxide.
The growth of plant species in Eastern Siberia during growing season isprovided by high rates of photosynthesis and transpiration at relatively low dark
expenses on respiration and maintenance. High inter annual variability ofphotosynthesis and dark respiration testifies to high adaptability of plants to the specificconditions of cryolithozone.
The productive process of plant species in Eastern Siberia is limited both byendogenous (stomatal conductance) and exogenous (provision with moisture andnutrients, nitrogen specifically) factors.
Permafrost forest and tundra ecosystems at present are estimated by carbon
budget as areas of significant carbon sink. However, under predicted climate warming,
their functions as carbon absorbers will essentially depend on the result of coordinationof antagonistic processes: 1) increasing of carbon accumulation owing to prolonged
vegetative period and elevated summer air temperatures; 2) frequency raise of forest
fires that result in increased carbon dioxide emission into the atmosphere.

㻕㻗㻪㻘㻐㻲㻖
G5–O3

ESTIMATING LARGE SCALE, REGIONAL, NET CO2 AND
CH4 FLUXES USING NESTED TOWER, AIRCRAFT FLUX,REMOTE SENSING, AND MODELING APPROACHES
Walter Oechel1, Donatella Zona1,2, and Cove Sturdevant1
1

San Diego State University, San Diego, CA, USA

2

University of Sheffield, Sheffield, UK

Estimating current and predicting future greenhouse gas fluxes from the Arctic isof great importance but is also exceedingly difficult.

In addition to remotelocations, logistic limitations, and difficult environmental conditions, especiallyduringnon-summer

periods,

landscapeheterogeneity

makemeasuring,

quantifying, and modeling greenhouse gas fluxes challenging.

Here weinvestigate some of the implications of landscape heterogeneity on GHG fluxes in
the Arctic, and consider how these can be measured and scaled to better informcurrent and future generations of land surface models dealing with arctic regions.
Landscape heterogeneity and microtopography affect processes that control CO2
and CH4 fluxes in a non-linear fashion.

It is therefore currently not possible todescribe, “average conditions” or “average responses” to a change in temperature
or moisture for a region of the Arctic that adequately describes current or predicts
future fluxes.

A combination of measurements from plot to aircraft scales andnested models can be used to evaluate current understanding and develop new
algorithms for the next generation of LSM for Arctic areas.

㻕㻘G5-O4
Cancelled

G5–O5㻪㻘㻐㻲㻘,PSDFWRI&OLPDWH&KDQJHRQHFRV\VWHPIXQFWLRQLQJDQG*+*
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G5–O6

REMOTE SENSING OF DECIDUOUS SHRUBS AND
PHYTOMASS IN ALASKAN ARCTIC TUNDRA
Keiji Kushida1, Satoru Hobara2, Shiro Tsuyuzaki3, Yongwon Kim4,
Manabu Watanabe5, Koichiro Harada6, Gaius R. Shaver7, Masami Fukuda8
1

Center for Far Eastern Studies, University of Toyama,
Faculty of Environment System, Rakuno Gakuen University,
3
Graduate School of Environmental Science, Hokkaido University,
4
International Arctic Research Center, University of Alaska Fairbanks,
5
Earth Observation Research Center, Japan Aerospace Exploration Agency,
6
School of Food, Agricultural and Environmental Sciences, Miyagi University,
7
The Ecosystems Center, Marine Biological Laboratory,
8
Department of Urban Management, Fukuyama City University,
E-mail address of corresponding author: kkushida@sci.u-toyama.ac.jp
2

The relationships among spectral indices, phytomass, and plant functional
types were determined through field observations of moist acidic tundra (MAT),
moist non-acidic tundra (MNT), and heath tundra (HTT) in the Toolik Lake Long
Term Ecological Research (LTER) site and sedge-shrub tundra (SST) in the Arctic
National Wildlife Refuge (ANWR), Alaska, USA. For MAT, MNT, and HTT, among
aboveground phytomass, aboveground vascular phytomass, and vascular plant
green phytomass, the last showed the best fit to an exponential function of thenormalized difference vegetation index (NDVI). Overall, the vascular plant green
phytomass was more strongly correlated to exponential functions of NDVI andtwo-band enhanced vegetation index (EVI2) (The coefficients of determination(R2) of 0.59 and 0.57, respectively) than to the other spectral indices. On the other
hand, for deciduous shrub green phytomass, the strongest correlation was withthe product of an exponential function of EVI2 and a spectral index (B+G–
R)/(B+G+R) (DSI, R2 of 0.66). Here, B, G, and R denote the blue, green, and red
bands, respectively. Results offer empirical evidence that a new spectral index
DSI provides the distributions of deciduous-shrub and leaf carbon and nitrogenturnovers, which influences on the interactions between the tundra ecosystems
and the atmosphere.

㻕㻛㻪㻘㻐㻲㻚
G5–O7
The climatic effect to North Eurasia ecosystems. Analysis
of 30-years satellite data
Vladimir ElsakovInstitute of biology, Syktyvkar, 167610 Kommunisticheskaja 28, Russia
elsakov@ib.komisc.ru
The temporal series of satellite images NOAA-AVHRR (1982-2006 years
period, 15 days periodicity), SPOT-Vegetation (1998-2004 years, 10 days
periodicity), Terra-MODIS (2000-2009 years, 16 days periodicity), Landsat(1973-2010 years, episodically) were used for selection of statistically significant
trends of natural positive and negative dynamics of vegetation production. The
selected plots of North-Europe Russia were investigated by geobotanical and     $   
mainly related with growing amount and biomass of shrubs in areas with constantpermafrost soils. On basis of comparable analyses of time-series satellite data wasdeveloped technology for quantitative estimation of features of vegetation in model
area (carbon accumulation, projective chlorophyll content, biomass, productivity).
Estimation of seasonal changes of parameters of native vegetation for years of first
decade of 2000 demonstrate more stable level of variations for area then earlysupposed. The trend of increasing of aboveground green biomass in this regions isnear 7-30 kgC*ha per year -1. The investigation was supported by program of      "    !          #12--4-1018).


The model of intensity of projective chlorophyll dynamic changes in vegetation for North
Eurasia for 2000-2011. The MODIS satellite data.

㻕㻜㻪㻘㻐㻲㻛
G5–O8
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S2–O1㻖㻔S2–O2㻖㻕

S2–O3㻖㻖

S2–O4㻖㻗

S2–O5㻖㻘

S2–O6㻖㻙㻪㻖㻐㻲㻔G3–O1

GROUND THERMAL REGIME AND ACTIVE LAYER THICKNESSMONITORING AND MODELLING IN THE NORDIC AREA
B. Etzelmüller1, H. H. Christiansen2, K. Gisnås1, K. Isaksen3, T.V. Schuler1, S.
Westermann1
1

Department of Geosciences, University of Oslo, Oslo, Norway

2

The University Centre in Svalbard (UNIS), Longyearbyen, Norway

3

Norwegian Meteorological Institute, Research and Development Department, Oslo,

NorwayCorresponding author: bernde@geo.uio.noSince 2001 numerous shallow boreholes were equipped to monitor groundtemperatures in the Nordic area, especially in Norway, Svalbard and Iceland. The total
number of monitored boreholes is 42, of which 4 are located in Iceland, 20 in southern
Norway, 16 in northern Norway and 12 in Svalbard. Most of these boreholes in northern
Norway and Svalbard were established during the IPY campaign 2007-2009. They are
set up to characterize the ground thermal regime in different environmental settings
along altitudinal and continental transects, and to validate spatially distributed,
equilibrium and transient permafrost models. Also as an important and integrative part of
the IPY activities the Norwegian permafrost database, NORPERM was established.
Most of the Norwegian permafrost data are today archived in the database, which islocated at the Norwegian Geological Survey (NGU).
Permafrost data were used to calibrate a transient heat flow model for altogether
29 of our sites all over the study area. The model was forced with meteorological dataover various time periods, ranging from the beginning of the instrumental data record at
the end of the 18th century to down-scaled projections of climate scenarios for the future(2100). The results illustrate the potential evolution of permafrost conditions and the
response to climate perturbations in sub-arctic mountains and high-arctic environments.
Also the data were used to validate numerical spatial permafrost models for Norway.
Here we present the updated permafrost thermal state as observed in theborehole network, along with modeled ground temperature and active layer thickness(ALT) development since the end of the Little Ice Age and their potential future evolution.
Also new spatial permafrost maps based on equilibrium and transient thermal modelingfor the Nordic area will be presented.

㻖㻚㻪㻖㻐㻲㻕G3–O2

PERMAFROST AND ACTIVELAYER MONITORINGNETWORK IN ALASKAN COMMUNITIESYoshikawa, K.1, Harada. K. 2, Iwahana, Go. 1, and Khalilova, J.3
1

Water and Environmental Research Center, Institute of Northern Engineering
University of Alaska Fairbanks, PO Box 755860 Fairbanks Alaska 99775-5860

2

Department of Environmental Sciences, School of Food, Agricultural andEnvironmental Sciences, Miyagi University, Sendai Japan

3

Geocryology laboratory, Sergeev Institute of Environmental Geoscience, Russian
Academy of Sciences, Moscow Russia

kyoshikawa@alaska.edu
The presence or absence of frozen ground has a strong effect on hydrology.
Frozen soil acting as an impermeable layer affects water availability to rootsystems of plants and the recharge of groundwater reservoirs. The frost tube
(active layer monitoring) program has been a great success in Alaskancommunities because it is relatively easy to implement, is cost-efficient, and is ahighly dynamic student activity. We have installed over 200 communities for asmall one-channel data logger connected to an ground temperature sensor next
to the frost tube. From the ground surface temperature data, freezing °C*days(freezing index) and thawing degree-days (thawing index) as well as mean annual
temperature can be calculated. This program reveals much of the thermal
structure of ground in Alaska, especially in many of the remote communities on
the southern boundary of permafrost (i.e., the northern end of the seasonal frost
region). Though there are many interesting aspects to this program, here we
discuss (1) the distribution of the maximum freezing and thawing layer thickness,and (2) freezing and thawing °C*days ground surface distribution in Alaska.

㻖㻛㻪㻖㻐㻲㻖
G3–O3

THERMAL STATES OF MONGOLIAN PERMAFROST AND
DEPLYOYING PERMAFROST OBSERVATORIES OVER THE
ARCTIC
M.Ishikawa1,2, K.Yoshikawa3, Y.Jambaljav4, N.Sharkhuu4, I.Yamahashi1,
S.Westermann5, B. Etzelmüller5, M.N.Zheleznyak6, S. Laxton7
1

Hokkaido University, Sapporo, Japan

2

Japan Agency of Marine-Earth Science and Technology, Yokosuka, Japan

3

University of Alaska, Fairbanks, USA

4

Institute of Geography, MAS, Ulaanbaatar, Mongolia

5

University of Oslo, Norway

6

Melnikov Permafrost Institute RAS, Yakutsk, Russia

7

Yukon Geological Survey, Canada

mishi@ees.hokudai.ac.jp
Permafrost has been degrading over large areas of the world, although thewarming rates show large spatial variations. Hence, it is important to organize andsustain to monitor the long-term thermal state of permafrost in various natural
settings. We have been improving permafrost network over Mongolia, establishing
new boreholes and recovering boreholes abandoned in the past. Currently
available datasets showed that warming rate ranges between 0.01 and 0.03°C/a,
and is more pronounced in the northern provinces with continuous permafrost.
Permafrost partly disappeared at the southern boundary of the discontinuous
permafrost in recent 30 years. Beside these country-scaled dynamics, strong
influences of local geographic variations on permafrost temperatures could beobserved. Cold permafrost occurs beneath topographic depressions, within
ice-rich soils, and under forested slopes. Further applications of these boreholedata are to develop high resolution permafrost map and to model future
distribution of permafrost.
The permafrost dynamics over Mongolia would be the epitome of those inglobe, since they involve the features of continuous, discontinuous, sporadic andmountain permafrost even in a small areas. Under the umbrella of GRENE andinternational collaborations, we are deploying permafrost observatories in Siberia
and Canada where the spatial density of permafrost network is currently sparse.

㻖㻜㻪㻖㻐㻲㻗G3–O4

PERMAFROST MAP IN RUSSIA USINGCOMMUNITY-BASED PERMAFROST AND ACTIVE LAYERMONITORING NETWORK
Khalilova, Y.1, Sergeev, D.1, Yoshikawa, K.2
1

Geocryology laboratory, Sergeev Institute of Environmental Geoscience, RAS,

Ulansky pereulok 13, building 2, P.O.Box 145, 101000 Moscow, Russia
2

Water and Environmental Research Center, Institute of Northern Engineering

University of Alaska Fairbanks, PO Box 755860 Fairbanks Alaska 99775-5860
Stanilovskaya@geoenv.ru

In 2008, an approach to mapping permafrost based on thermal conditions wasintroduced during the Ninth International Conference on Permafrost (Jorgensen etal., 2008). This approach maps permafrost distribution using the annual mean air
temperature model (PRISM) and surficial geology (the GIS platform). A thermal
offset or gap occurs between air and ground surface temperatures mainly becauseof snow cover or other thermal effects. Use of the annual mean groundtemperature model instead of air temperature will produce better results. Ourcommunity-based permafrost and active layer monitoring network measuresground temperature year-round at hundreds of locations. These data are useful for
calibration or verification of the new model. The original objective of thisnetwork was to establish long-term permafrost monitoring sites near communities
and schools so that students and teachers could be involved in installation of themonitoring equipment and data gathering. Permafrost condition is an important
indicator of climate change, since permafrost is directly influenced by climate.
Permafrost affects local ecosystems and hydrological regimes, and is a factor innatural disasters related to ground stability. Once we develop a station, data are
available to the public for science, engineering, and education purposes. An
important project related to the permafrost monitoring stations is the
mapping/modeling of permafrost. Our community-based monitoring system willcontribute to the production of a more-accurate permafrost map. With improved
mapping/modeling in mind, we plan to finish the Alaska permafrost map, thendevelop the same method in Russia as in Alaska by establishing monitoring
stations in Sakha Republic and other parts of Russia. To begin with, however, we
will focus on establishing this network over the next several years.

㻗㻓㻪㻖㻐㻲㻘
G3–O5

Cancelled

PARAMETRIZATION OF RUNOFF FORMATION MECHANISMS IN MOUNTAINOUS
PERMAFROST CONDITIONS OF RUSSIA AND CANADA (THE KOLYMA WATERBALANCE STATION AND WOLF CREEK RESEARCH WATERSHED)
Olga Semenova1,2,3, Lyudmila Lebedeva4,2,3
1
*LGURWHKSURHNW/WG

+\GURJUDSK0RGHO5HVHDUFK*URXS
6WDWH+\GURORJLFDO,QVWLWXWH1DQVHQ&HQWUH
6W3HWHUVEXUJ5XVVLDRPDNDULHYD#JPDLOFRP
The parameterization of process-based hydrological models reflects natural conditionsof runoff formation processes and should be developed and tested on the basis ofdetailed and long-term measurements at research watersheds. Very limited number ofsuch catchments exists in the permafrost zone.
The aim of the study was the development of parameterization schemes describing
mountainous territories of Russian Northern East and Canadian part of the Yukon Riverbasin for the purposes of hydrological modelling.
The study included the following steps: i) comparative analysis of flow formation
processes in two research watersheds of Russia and Canada at slope and catchment
scales ii) deriving soil and vegetation parameters by additional sources of informationand modelling experiments at slope scale iii) transferring the parameters from slope tocatchment scale and performing runoff simulations iiii) analysis of the results andconclusion about workability and limitations of developed parameterization scheme.
Two research watersheds, the Kontaktovy Creek and the Wolf Creek basins (21.2 and195 km2 respectively) were studied. Although both of them are covered by permafrost
and relate to the zone of mountainous taiga and tundra, they have significant
differences in runoff formation mechanisms.
The Kontaktovy Creek basin is characterized by continuous permafrost while in the Wolf
Creek basin permafrost occupies only northern slopes and headwaters. It leads to
predominance of surface and shallow subsurface flow formed in active layer at the
Kontaktovy Creek watershed, while the underground flow dominates in the Wolf Creekbasin. At both watersheds different slopes show specific thermal and water regime due
to difference in solar radiation income and dominant landscapes.
Observable land cover properties were derived from literature review and used as themodel parameters to simulate soil thaw/freeze depths, soil moisture and temperature,snow accumulation and melting.
Soil and vegetation parameters were initially refined at slope scale on the base ofmultiple modelling experiments and then transferred to the watershed scale withoutchange. Good agreement between observed and simulated runoff confirmed theeffectiveness of the parameterization.
The Hydrograph model applied to both watersheds at slope and catchments scales is aprocess-based hydrological model. It adequately describes land hydrological cycle
based on standard daily input information. Sufficient algorithm of water and heat
dynamics in the soil enables to use this model in various condition of permafrost.
We propose that gained parameterization scheme and the Hydrograph model can beapplied to ungauged and poorly gauged basins at the Yukon River in Canada and theUpper Kolyma River in Russia.
㻗㻔㻪㻖㻐㻲㻙
G3–O6

TEMPORAL SEQUENCING OF ANNUAL SPRING RUNOFFIN FOUR MAJOR ARCTIC-DRAINING RIVERS
Ahmed, R.1,

Prowse, T.D.1,2,

Dibike, Y.B.2, Bonsal, B.R.3

1

Water and Climate Impacts Research Centre, University of Victoria, Victoria,

Canada.
2

Water and Climate Impacts Research Centre, Environment Canada, Victoria,

Canada.
3

National Hydrology Research Centre, Environment Canada, Saskatoon, Canada.

Corresponding author email: roxannea@uvic.ca
Warming in the Arctic has significance as an indicator of global climatechange and through feedbacks to the global climate system.

The influx offreshwater to the Arctic Ocean has the potential to influence global climate
through modification of the intensity of the thermohaline circulation. Thisemphasizes the importance of understanding climate-discharge linkages in
Arctic-draining rivers, which are the dominant source of freshwater input to the
Arctic Ocean. To date, no research has evaluated trends in the magnitude andsequential timing of the spring freshets – the dominant hydrologic event occurringon these nival river systems – or of the atmospheric circulation patterns that
control them. To address these shortcomings, historic daily discharge data fromselected hydrometric stations within the four largest Arctic-draining watersheds(Mackenzie, Ob, Lena, Yenisei) have been analyzed to extract data about thetiming, magnitude and characteristic shapes of the spring freshet hydrographs.
Discussion of results focus on: the temporal sequencing of spring discharge atstations draining directly to the Arctic Ocean along the Mackenzie, Ob, Lena, andYenisei rivers; the discharge linkages with controlling patterns of temperature andprecipitation; and the major atmospheric teleconnection patterns associated withextreme high and low flow years.

㻗㻕㻪㻖㻐㻲㻚
G3–O7

ICE MOVEMENT IN THE LENA RIVER AND THE TYPOLOGY OF
SPRING FLOOD: AN INTERPRETATION OF LOCAL SOURCESINTEGRATED WITH SATELLITE IMAGERY USING A
MULTIDISCIPLINARY APPROACH
Hiroki Takakura1, Yasuhiro Yoshikawa2, Manabu Watanabe3, Toru Sakai4, Tetsuya
Hiyama4
1
Center for Northeast Asian Studies, Tohoku Univerisity, Kawauchi 41, Aobaku, Sendai,
980-8576, Japan, hrk@m.tohoku.ac.jp
2
Civil Engineering Research Institute for Cold Region, Hiragishi 1-3-1-34, Toyohiraku,
Sapporo, 062-8602, Japan, yoshikawa84@gmail.com
3
Earth Observation Research Center, Japan Aerospace Exploration Agency, 2-1-1
Sengen, Tsukuba, Ibaraki 305-8505 Japan, watanabe.manabu@jaxa.jp
4Research Institute for Humanity and Nature, 457-4 Motoyama, Kamigamo, Kitaku, Kyoto,603-8047, Japan, torus@chikyu.ac.jp, hiyama@chikyu.ac.jp
Spring flooding of northern rivers in both Arctic and sub-arctic regions is a regular seasonal
event. As snow and ice thaw, floating freshwater ice appears in the rivers and flooding
occurs, which is critical for the regional ecosystem and for water circulation. Theoretically,
climate change should have some effect on this phenomenon, but due to regionalvariations and the complex interplay of elements, scientific data on how the climate isaltering the freshwater ice process is still unclear. At the same time, since the spring river ice
process and flooding have definite effects on human societies, these are now becoming
issues of focus and urgency for social scientists and disaster management policymakers.
From the human-dimension perspective, river ice is an important regional infrastructure
because it is used for major winter transportation and local subsistence activities.
Understanding the process of river ice breaking and consequent flooding is important forinterdisciplinary area studies because they are closely related to local societal-technologicalaspects and the regional environment. This paper explores the concrete process of springflooding through a case study of the Lena River in eastern Siberia. Recently, the frequency
of disastrous spring flooding has increased in this region. Although a decisive explanation is
not yet available, the local government is urgently demanding adequate policies andmeasures. In what conditions does the process of spring flooding develop in the Lena
River? We will describe concrete processes such as ice movement and velocity, the locusof the flooding outbreak, and the disastrous results. The method of analysis is aninterpretative approach using multi-disciplinary data from satellite imagery, literature sources,
and fieldwork. At the same time as Landsat or large scale resolution images of flooding
from a bird’s-eye view provides the general outlook, the information of ice monitoring andflood reporting from local newspapers will be visualized using GIS software (Google Earth),and ALOS satellite or high resolution imagery of a particular flooding event is interpreted
based on anthropological field data. Through these means, we identify several types offlooding and examine their implications for human societies.

㻗㻖㻪㻖㻐㻲㻛
G3–O8

WATER BALANCE OF ARCTIC WETLANDS WITH
DIFFERING ICE WEDGE POLYGON TYPE
Anna K. Liljedahl1,2,Ronald P. Daanen1,

Cathy J. Wilson3, Jörg Schulla4,

Larry D. Hinzman2
1

Water and Environmental Research Center, University of Alaska Fairbanks

2

International Arctic Research Center, University of Alaska Fairbanks

3

Los Alamos National Laboratory, Los Alamos

4

Hydrologic Software Consultant, Zurich

akliljedahl@alaska.edu

Ice wedge polygons are common in landscapes underlain bypermafrost. Still, their role on watershed-scale hydrology is constrained. We
combined field measurements with mass and heat transfer modeling to assess
the effect of ice wedge polygon type on landscape-scale hydrologic fluxes andstores. The physically-based model WaSiM was applied to airborne LiDAR
and schematic DEMs, and forced by climate data from an Arctic wetland,
Barrow, Alaska. Simulations and field measurements were concentrated tofour sites, i.e. landscape types: high-centered, low-centered, and two
transition polygon sites (the latter having both low-centers and troughs). Model
simulations suggest that low-centered polygons, through elevated rims,
reduce runoff while increasing evapotranspiration and water storage. The
high-centeredpolygonlandscapefavorsrunoff,while

storageandevapotranspiration drastically decrease. Continuous field measurements inneighboring, individual ice wedge polygons presents drastically different
seasonal variability in water tables between study sites, despite the samelandscape-scale end-of-winter snowpack water storage. It is evident from thefield and modeling analyses that microtopography plays an important role on
low-gradient Arctic wetland watershed-scale hydrology. Further, the finemicrotopographical variability results in hydrologic characteristics that canpresent important geomorphological feedbacks. A shift in ice wedge polygon
type could potentially dominate the initial effects of altered climate on Arctic
wetland hydrology.

㻗㻗㻪㻖㻐㻲㻜
G3–O9              
                    

 

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G3–O10ICE COVER OF EURASIAN LAKES AND INLAND SEAS
FROM SATELLITE AND IN SITU OBSERVATIONS
A. V. Kouraev1,2, M.N. Shimaraev3, F. Rémy1,4, M.A. Naumenko5,,A. Suknev61) Universite de Toulouse; UPS (OMP-PCA), LEGOS, Toulouse, France2) State Oceanography Institute, St. Petersburg branch, Russia
3) Limnological Institute, Siberian Branch of RAS, Irkutsk, Russia ,4) CNRS; LEGOS, F-31400 Toulouse, France,5) Limnology Institute of the RAS, St. Petersburg, Russia,6) Great Baikal Trail Buryatiya, Ulan-Ude, Russia
Because of its response to regional and global variations in the climate
system, arctic and sub-arctic lakes and internal seas are not only an integrator ofclimate processes, but also strong indicator of existing or potential change. It is
important to well understand what are temporal and spatial scales of variability ofnatural parameters, what are teleconnections, feedbacks and mechanisms
responsible for the changes, what are natural and anthropogenic causes ofrecent and historical changes in the hydrophysical and meteorologicalparameters. Changes in natural parameters are important for human activity(navigation, transport, fisheries, tourism etc) and affect large population living
around.
We present studies of ice and snow cover of continental water bodies
using the synergy of more than 15 years-long simultaneous active (radar
altimeter) and passive (radiometer) observations from radar altimetric satellites(TOPEX/Poseidon, Jason-1, ENVISAT and Geosat Follow-On) complemented by
SSM/I passive microwave data. Five largest Eurasian continental water bodies Caspian and Aral seas, Baikal, Ladoga and Onega lakes are selected as
examples. An ice discrimination approach based on a combined use of the data
is presented, as well as validation of this approach using in situ and independent
satellite data in the visible range. We then analyse the long-term evolution of ice
conditions for these lakes and inland seas using historical data and recent
satellite observations. We also present our results of the field studies on thelakes Ladoga and Baikal.
We address another interesting phenomenon - formation of giant rings on
Baikal Lake ice. These rings (diameter 5-7 km, thickness of dark layer - 1 - 1.8km) have almost perfect circular shape. The rings have been observed since theearly 1970ies by satellite imagery in various regions of the lake. We present
several existing hypotheses of the origin of these rings and discuss strengths andweaknesses of each hypothesis. We present observation of the formation,
development and disappearance of these rings using various satellite data. We
discuss the conditions needed to create and maintain these rings, the timing ofand duration of their existence, as well as horizontal and vertical structure of ice
and snow cover and of temperature and conductivity before and during theappearance of rings.
This research has been done in the framework of the Russian-Frenchcooperation GDRI "CAR-WET-SIB", French CNES TOSCA AO, CNRS-Russia
PICS BALALAIKA, Russian FZP 1.5 and FP7 "MONARCH-A" projects.

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AEROSOL CHARACTERISTICS OVER NORWEGIANARCTIC: RESULTS FROM INDIAN SCIENTIFIC
EXPEDITIONS
Mukunda M Gogoi1*, S Suresh Babu1, K Krishna Moorthy1, Jai Prakash
Chaubey1, Vijayakumar S Nair1, Manoj M R1, Sobhan Kumar Kompalli1, Lakshmi
N B1, Roseline C Thakur2, Thamban Meloth2, S Rajan2
1

Space Physics Laboratory, Vikram Sarabhai Space Centre,
Thiruvananthapuram-695022, India

2

National Centre for Antarctic and Ocean Research, Vasco da Gama,
Goa-403804, India
E-mail: dr_mukunda@vssc.gov.in; mukunda.mg@gmail.com

In the context of global climate change, there is an increased need inunderstanding the role of atmospheric aerosols in arctic atmosphere in changing
the snow Albedo, phenomenon like ‘Arctic haze’ and ‘thinning of Arctic Sea’ andperturbation to the radiation balance in the Arctic region. As a part of Indian
Scientific Expedition to Arctic, extensive measurements of scattering andabsorption properties of aerosols have been in progress at Ny Alesund (78.9°N,
11.9°E) in Svalbard archipelago of Norwegian Arctic since June 2011. The
results from the year round measurements indicate that the mass concentrationof Black Carbon (BC) aerosols showed large annual variation with values as low
as ~5 ng m-3 to as high as ~ 300 ng m-3 (during winter/spring). Similarly, thescattering coefficients also showed significant annual variation with higher values(~ 30 Mm-1) during the winter and spring. However, the aerosol single scattering
albedo was lower (as low as 0.85) during the summer. In addition, theinvestigation of aerosol black carbon in the snow samples collected around NyAlesund during the onset of Arctic spring (2012) indicates that the mean
concentration of BC in snow varied from ~ 1 to 5 ppb; while the corresponding
atmospheric BC varied from ~ 25 ng m-3 to 50 ng m-3. Since there was no
significant snowfall during this period, the observed BC in snow is usuallyassociated with dry deposition. The details of the observational program and theresults will be presented.

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G1–P3
COMBINED MEASUREMENTS OF GRAVITY WAVES WITH
AN AIRGLOW IMAGER AND ALOMAR LIDARS IN NORWAY
S. Suzuki1, F.-J. Luebken2, G. Baumgarten2, N. Kaifler2, R. Eixmann2,
B. P. Williams3, and T. Nakamura4
1

Solar-Terrestrial Environment Laboratoty, Nagoya University (Nagoya, Japan)

2

Leibniz-Institute of Atmospheric Physics (Kühlungsborn, Germany)

3

GATS, Incorporated (Boulder, CO, United States)

4

National Institute of Polar Research (Tachikawa, Japan)

shin@stelab.nagoya-u.ac.jp
To investigate the vertical propagation of gravity waves from the lower tothe upper atmosphere, combined measurements with an airglow imager andlidars were carried out at the Arctic Lidar Observatory for Middle Atmosphere
Research (ALOMAR) station (69.3ºN, 16.0ºE) in Norway. Airglow imaging reveals
the two-dimensional structure of gravity waves in the mesopause region, while the
ALOMAR Rayleigh/Mie/Raman (RMR) lidar and sodium lidar provide the verticalstructures between the stratosphere and the lower thermosphere. On 26
November 2010, the imager identified a mesoscale gravity wave structure in thesodium airglow that had a horizontal wavelength of 277 km, a wave period of 59
min, and propagated northeastward at a phase speed of 78 m s1. Simultaneous
lidar measurements also showed upward wave signatures with a similar wave
period in the temperature perturbations; the vertical wavelength of the upward
wave seen in the temperature data is consistent with the dispersion relation for
gravity waves. Based on the combined measurements with the imager andsodium lidar, momentum flux of this gravity wave was estimated to be 1.0 m2 s2 atthe sodium airglow height. Ray-tracing analysis suggested that the observed
gravity wave was generated by a distortion of the polar jet at the tropopause via ageostrophic adjustment process.

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Variations of the polar lower thermosphere, mesosphere,
and ionosphere due to a SSW ~ A case study of theJanuary 2012 event~Nozawa1, S., T. Kawahara2, T. Tsuda3, T. Kawabata1, N. Saito4, S. Wada4,
Y. Ogawa3 and M. Tsutsumi3
1

STEL, Nagoya University
Shinshu University
3
NIPR
4
RIKEN
Corresponding author: nozawa@stelab.nagoya-u.ac.jp
2

Effects of Sudden Stratospheric Warming (SSW) on the Thermosphere have been
paid great attentions for last half decades in terms of the atmospheric vertical
coupling process. We report results of a case study of the January 2012 SSW
event based on observations made at Tromsø (69.6°N, 19.2°E). In Tromsø, wehave been conducting comprehensive observations using European Incoherent
SCATer (EISCAT) radars, MF radar, meteor radar (owned by NIPR), Fabry-Perot
Interferometer (FPI), aurora imagers, photometer, and sodium LIDAR. From 0739
UT on January 13, 2012 to 2300 UT on January 23, 2012, the EISCAT UHF radar
was operated with a scanning mode (so-called ip2 mode) and succeeded in
obtaining good quality data (ionospheric parameters above 90 km, and neutral
wind velocity between 90-120 km) over the time interval. The weather was good,
and then we succeeded in obtaining neutral temperature data for nine nights(January 13, 14, 17, 18, 19, 20, 21, 22, 23) by sodium LIDAR. MF and meterradars conducted wind observations in the mesosphere. We will show results ofa case study on this event, and discuss how the lower
thermosphere/mesosphere/ionosphere varied during the SSW event.

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SODIUM DENSITY VARIATION DURING AURORALPARTICLE PRECIPITATIONS
T. T. Tsuda1, S. Nozawa2, T. D. Kawahara3, T. Kawabata2, N. Saito4, S. Wada4,
S. Oyama2, Y. Ogawa1, S. Suzuki2, T. Takahashi2, T. Nakamura1
1

National Institute of Polar Research (Tachikawa, Tokyo, Japan)

2

Solar-Terrestrial Environment Laboratory, Nagoya Univ. (Nagoya, Aichi, Japan)

3

Faculty of Engineering, Shinshu Univ. (Nagano, Nagano, Japan)

4Advanced Science Institute, RIKEN (Wako, Saitama, Japan)

E-mail address of corresponding author: tsuda.takuo@nipr.ac.jp
Sodium atom layer is generally distributed at 80-100 km. One ofmysterious subjects on high-latitude sodium layers is relationship between auroral
particle precipitations and sodium atom layer variations. A previous study
suggested a sodium column density decrease during a geomagnetic active period
due to that the particle precipitations accompanied by electron density
enhancement could induce ionization of sodium atom through their ion-molecule
chemistry. Another study pointed a possibility of sodium density increase. For thisreason, it is suggested that precipitating particle bombardment on meteoric smoke
particles can sputter sodium atoms from the smoke particles. On the other hand,ionospheric electric fields, which may become more significant near auroral
precipitating regions, could induce ion motions (i.e. can generate sodium ion
convergence and/or divergence), and then also could affect generation and/or
loss processes of sodium atoms through their ion-molecule chemistry. Thus, forthe evaluation of the causarity, it is important to distinguish the effects of auroral
particle precipitations and ionospheric electric fields. Using a sodium lidar (which
was installed in early 2010) and European incoherent scatter (EISCAT) radar atTromsø, Norway (69.6ºN, 19.2ºE), we have investigated, for the first time, that theactual effect of the particle precipitation to the sodium density variations without
electric filed injection. In the nighttime observation on 24 January 2012, wedetected a significant decrease of sodium atom density coincied with electron
density enhancements (implying strong particle precipitations) and low ion
temperatures (implying no electric field injections). These results strongly
suggested that auroral particle precipitations induced sodium atom density
decrease.

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CURRENT STATUS OF THE STEL OPTICALOBSERVATIONS AT THE TROMSØ EISCAT RADAR SITE
Shin-ichiro Oyama1,
Yuichi Otsuka1,

Satonori Nozawa1,

Ryoichi Fujii1,

Kazuo Shiokawa1,

Toru Takahashi1

1Solar-Terrestrial Environment Laboratory, Nagoya University

soyama@stelab.nagoya-u.ac.jp
Solar-Terrestrial Environment Laboratory (STEL), Nagoya University has
operated various kinds of optical instruments for more than 10 years at theTromsø EISCAT (European Incoherent Scatter) radar site in Norway (69.6ºN,
19.2ºE), which is one of the state-of-art observatories for the upper atmosphericphysics at high latitudes. Seven instruments are now in operation regularly from
October to March: (1) a three-wavelength photometer (simultaneously measuring
the emission intensity of aurora at 427.8 nm, 630.0 nm, and 557.7 nm), which isfixed to look along the magnetic field line, (2) two digital cameras for monitoring
weather and aurora, (3) a proton all-sky camera (wavelength at 486.1 nm), (4)multi-wavelength all-sky camera (programmatically selecting one of the opticalfilters at 557.7 nm, 630.0 nm, near-infrared OH band, 589.3 nm, 572.5 nm, and732.0 nm), (5) a Fabry-Perot interferometer (programmatically selecting one of the
optical filters at 557.7 nm, 630.0 nm, and 732.0 nm), (6) a sodium LIDAR. All ofthem (except for the sodium LIDAR) are automatically operated. These
instruments have joined many campaign observations with the EISCAT radars,
rockets, satellites, and other ground-based instruments by adjusting theobservation mode. The quick looks are available to see on the web at:www.stelab.nagoya-u.ac.jp/~eiscat/data/EISCAT.html
This paper reports the current operation status and some new results of these
optical instruments until the end of 2012.

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CURRENT STATUS OF UPPER ATMOSPHERE PHYSICSOBSERVATION IN ICELAND IN 2012
Akira Kadokura 1, N. Sato 1, H. Yamagishi 1, Y. Tanaka 1, Y. Sato1, T. Koshida1,
M. Taguchi 2, T. Ono 3, T. Motoba 4, K. Hosokawa 5, Gunnlaugur Bjornsson 6
1

National Inst. of Polar Research, 10-3, Midoricho, Tachikawa, 190-8518, Japan

2

Rikkyo Univ., 3-34-1 Nishi-Ikebukuro,Toshima-ku, Tokyo 171-8501, Japan

3

Tohoku Univ., 6-3, Aoba, Aramaki, Aoba-ku, SendaiI 980-8578, Japan

4

The Johns Hopkins University Applied Physics Laboratory, 11100 Johns

Hopkins Road, Laurel, Maryland 20723, U.S.A.
5

Univ. Electro-Communications, 1-5-1 Chofugaoka, Chofu-shi 182-8585, Japan

6

Science Institute, University of Iceland, Dunhagi 3, IS-107 Reykjavik, Iceland

kadokura@nipr.ac.jp
Syowa Station (SYO) in Antarctica and Iceland in the northern hemisphere
are located at auroral latitudes, and in the geomagnetic conjugate relationship,
where both are connected with each other with a same magnetic field line.
Conjugate observations of auroral phenomena in Iceland have been carried out
since 1984 as a collaborative project between National Institute of Polar Research(NIPR), Japan and University of Iceland. At present, there are two observatories in
Iceland; Husafell (HUS) and Tjornes (TJR). Conjugate point of Syowa, which was
initially located between HUS and TJR in 1984, is now located just north-eastward
of TJR. Various ground-based instruments are operated now. We will show thecurrent status of the upper atmosphere physics observations in Iceland as of2012.

Fig.1. Map of Iceland.
Indicated are locations ofobservatories in Iceland(HUS, TJO, AED), andgeomagnetic traced
footprint of Syowa Station(star symbols) from 1980
to 2010.

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SOIL CARBON FLUX IN BLACK SPRUCE FOREST AFTERFOREST FIRE, INTERIOR ALASKA

Yongwon Kim1, Yuji Kodama2, Yoshinobu Harazono1, and Hiroki Iwata1
1

International Arctic Research Center, University of Alaska Fairbanks, Fairbanks,

AK 99775-7335, USA2

Arctic Environment Research Center, National Institute of Polar Research,

Tokyo 190-8518, Japan
E-mail: kimyw@iarc.uaf.edu
Northern boreal forests represent approximately 35% of the world’s forestand contain ca. 66% of the world’s forest soil carbon pools. Because boreal
forests uptake atmospheric carbon dioxide and slowly decompose litter, fibric andhumic substances, the ecosystems are known as carbon sinks.

Forest fire is amajor disturbance in boreal forests, with its occurrence closely coupled to climate
patterns, resulting in changes in Arctic climate. Here, we present soil carbon efflux
in burned black spruce forest with the succession on after 2004 forest fire that is
the most severe damaged year. After 5 years, we have measured soil carbon
efflux using automated chamber system that consists of 6 chambers (each threetransparent- and opaque-material), controller included data-logger, 12 solenoid
valves and pump, and thermocouples. Common hair moss (Polytrichum
commune) grew natural plant after the fire. The NPP (net primary productivity), Re(ecosystem respiration) and GPP (gross primary productivity; GPP = Re - NPP) of
the moss was measured using transparent- and opaque-material chambers,
which mean NEE, Re and GPP were -0.03±1.19, 1.09±0.71, and 1.12±1.51
gC/m2/sec, respectively. Mean microbial respiration after the fire 0.78±0.41
gC/m2/sec, averaged four chambers in no plants from August to October of2009. These carbon fluxes have exponential correlations to temperature,indicating the Q10 values on temperature of air, soil 5 cm and 10 cm below thesurface were 1.66, 2.73, and 3.23, respectively. NEP (net ecosystem productivity)of Common hair moss was roughly -0.81gC/m2/sec, suggesting the losing
carbon of 3.15 gC/m2 for 45-day. This data will compare with NEP by eddy
covariance tower.

㻔㻔㻙㻪㻘㻐㻳㻖
G5–P3

CRYOSPHERICAL COHESIVE REGIONS AS TERRESTRIALRESEARCH IN ALASKA FOR A COLLABORATIVEFRAMEWORK BETWEEN JAMSTEC AND IARC
Sugiura, K.1,2, R. Suzuki3, K. Saito2,3, A. Ito3, Y. Kim2, H. Park1, J. Cherry2,
J. Walsh 2, J. Cable2, S. Nagai3, T. Nakai2
1

Japan Agency for Marine-Earth Science and Technology (JAMSTEC), 2-15
Natsushimacho, Yokosuka 237-0061, Japan
2
International Arctic Research Center (IARC), University of Alaska Fairbanks, 930
Koyukuk Drive, Fairbanks, Alaska 99775-7340, U.S.A.
3
Japan Agency for Marine-Earth Science and Technology (JAMSTEC), 3173-25
Showamachi, Kanazawa-ku, Yokohama 236-0001, Japan
E-mail: sugiura@jamstec.go.jp (Sugiura, K.)
JAMSTEC-IARC Collaboration Study (JICS) is planned as a five-year project from2009 JFY through 2013 JFY. Our approach has been to carefully examine the ongoing
physical and biological processes and determine the underlying drivers and inherent
linkages among system components. Research has been conducted to understandmulti-scale interactions in the Arctic system, to quantify the impact of observing systemcomponents, and to utilize observations in tests and validation experiments for modelingand remote sensing. Providing the observation tower in the JICS supersite located to thenorth of Fairbanks, Alaska, is expected to contribute to a base for understanding terrestrial
processes and variation on a mesoscale. Simultaneously, regional field surveys havebeen carried out at selected areas in Alaska. This paper introduces investigations related
to the regional field surveys in Alaska.
Regarding ecosystem research, the above-ground biomass (AGB) of 29 forests
along the south-north transect which profiles from boreal forest to tundra in Alaska wasmeasured to construct the estimation algorithm of forest AGB by ALOS/PALSAR data. In
some forests, temporal biomass changes have been monitored. Regarding permafrost
research, physical properties of the surface and sub-surface have been measured at theinterior (taiga), western (tundra) and southern (maritime) coastal sites. Large variations
were found in near-surface soil thermal and hydrologic regime across short distances, with
wet troughs experiencing freeze-up about a month later that the dry and exposed rims.
The climatic gradient of soil and snow property that will be used in large-scale climate
models has been surveyed by in-situ measurements and by lab analysis. Regarding snow
cover research, snow surveys have been continuously carried out and several time-lapse
cameras were installed in a longitudinal section of Alaska. A blowing snow sensor was
installed at the northern tundra site. In addition, a physically basedsnow-atmosphere-ground-vegetation model has been developed, with inclusion of
blowing snow processes. Regarding greenhouse gas research, diurnal and seasonalvariations of floor CO2 exchange in the interior taiga site have been continuously
measured. A process-based terrestrial ecosystem model simulated greenhouse gas
budget of northern terrestrial ecosystems, daily soil respiration, and global distribution ofannual CH4 emission from wetlands and paddy fields. Regarding hydrological research, a
coupled hydrological and biogeochemical model (CHANGE) simulated inter-annual
variations of hydrological processes over the pan-Arctic. A seesaw pattern in interannual
variations of active layer thickness (ALT) was found between Lena and Mackenzie basins,
which was significant when the Arctic air temperature entered into a warming phase,
implicated with changing snow cover and soil moisture. While it is widely believed that ALT
will increase with global warming, this hypothesis may need modification because the ALTshows responses to variations in snow depth and soil moisture that can over-ride theeffect of air temperature.
It is necessary for systematic framework to improve understanding of linkages andfeedbacks among Arctic climate system components on a mesoscale to a synoptic scalein future, in addition to further continuous data collection and analysis.

㻔㻔㻚㻪㻘㻐㻳㻗
G5–P4

THE JAMSTEC-IARC SUPERSITE ENHANCESUNDERSTANDING OF THE ARCTIC CLIMATE SYSTEM– BIOGEOCHEMICAL OBSERVATIONS –Rikie Suzuki1, Yongwon Kim2, Shin Nagai1, Hideki Kobayashi1, Taro Nakai2, andAkihiko Ito3
1
Research Institute for Global Change, Japan Agency for Marine-Earth Scienceand Technology (JAMSTEC), 3173-25 Showamachi, Kanazawa-ku, Yokohama
236-0001, Japan
2
International Arctic Research Center (IARC), University of Alaska Fairbanks, 930
Koyukuk Drive, P.O. Box 757340, Fairbanks, Alaska 99775-7340, U.S.A.
3
Center for Global Environmental Research, National Institute for Environmental
Studies, 16-2 Onogawa, Tsukuba, Ibaraki 305-8506, Japan
E-mail: rikie@jamstec.go.jp (Rikie Suzuki)
Under the JAMSTEC-IARC Collaboration Study (JICS), the supersite wasestablished in the Poker Flat Research Range (PFRR) of the University of Alaska
Fairbanks in 2010, and observations on biogeochemical studies in the black
spruce forest have been intensely carried out in addition to observations for hydro-meteorological studies. This paper introduces biogeochemical observations
which are being taken place at the JICS supersite in PFRR.
Tree census survey was conducted at the 30m x 30m quadrat of the black
spruce forest near the JICS tower in July 2010 to delineate the forest structure.
The result of the census survey clarified that the density of tree stand (over 1.3m)
was 3967 tree ha-1. Also we cut down 16 trees in the forest in August 2012, andmade the allometry equation for the estimation of the leaf area index and theabove-ground biomass of black spruce tree. The forest landscape is always being
monitored by the automatic digital fisheye camera installed on the top of the 17m
JICS tower with 3 hours interval. Those pictures by the camera provide us valuable ideas to interpret the satellite data that show the seasonal change. The
floor-level carbon dynamics are monitored with the automated open/close chamber (AOCC) system that has 16 chambers in the forest. By combining thefloor-level flux data with the atmosphere-level flux data measured at the tower, theroles of forest canopy and floor in gas exchanges will be elucidated.
These biogeochemical observations are integrated with the hydro-meteorological observations of thesupersite, and the data will be utilized
for various studies included the studyof biogeochemical modeling such as
Vegetation Integrative Simulator forTrace Gases (VISIT). Moreover theknowledge and understandings which
are created based on the supersite Black spruce forest in the JICS supersite
observations will substantially enhance viewed from the top of the 17m JICS
the study on Arctic climate system.
tower (July 2010).

㻔㻔㻛㻪㻘㻐㻳㻘
G5–P5

THE JAMSTEC-IARC SUPERSITE ENHANCESUNDERSTANDING OF THE ARCTIC CLIMATE SYSTEM– HYDRO-METEOROLOGICAL OBSERVATIONS –
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1

International Arctic Research Center (IARC), University of Alaska Fairbanks, 930
Koyukuk Drive, Fairbanks, Alaska 99775-7340, USA
2
Research Institute for Global Change (RIGC), Japan Agency for Marine-Earth
Science and Technology (JAMSTEC), 2-15 Natsushima-Cho, Yokosuka,
Kanagawa 237-0061, Japan
3
Research Institute for Global Change (RIGC), Japan Agency for Marine-Earth
Science and Technology (JAMSTEC), 3173-25 Showamachi, Kanazawa-ku,
Yokohama, Kanagawa 236-0001, Japan
E-mail: tnakai@iarc.uaf.edu, taro.nakai@gmail.com (Taro Nakai)$V WKH NH\ REVHUYDWLRQDO UHVRXUFH RI WKH -$067(&,$5& &ROODERUDWLRQ
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G5–P6

ENVIRONMENTAL QUALITY MONITORING OF
BIODIVERSITY WITHIN CRYOLITHOZONE OF THE
SAKHA REPUBLIC (YAKUTIA) IN THE CONDITIONSOF ECONOMIC USE AND GLOBAL CLIMATE CHANGE
*1

*1

*2

N.G. Solomonov , I.M. Okhlopkov , S. Tatsuzawa
Institute for Biological Problems of Cryolithozone SB RAS
Lenin Avenue 41, 677980, Yakutsk e-mail: imokhlopkov@yandex.ru*2
Graduate School of Letters, Hokkaido University, Kita-ku, Sapporo 060-0810,
Japan
*1

Today the Sakha Republic (Yakutia) establishes its own network of ecologicalmonitoring because there is not any biosphere nature reserve over the spacious territoryof the republic.
It includes the network of hydrometeorological stations under
Rosgidromet and observation stations belonging to the system of the Ministry of Nature
protection of the Republic. In 2008 a public institution “Republican Information AnalyticalCenter of Ecological Monitoring” was organized under the auspices of the MNP SR(Ya).
There are also polygons performing their activity in Sakha affiliated to the Permafrost
Institute SB RAS on monitoring concerning the state of permafrost grounds, to theInstitute of Cosmic Research and Aeronomy SB RAS on monitoring of solar-terrestrial
relation, space weather, thunderstorm activity and condition of works and spread of forest
fires, to the Institute for Biological Problems of Cryolithozone SB RAS on monitoring ofgreenhouse effect, carbon emission, photosynthetic intensity, structure and functioning ofsubarctic, mountain and alas-taiga ecosystems. There are 2 state nature reserves and a
lot of specially protected natural territories under the status of the Republic, which
perform their activity on the ecological monitoring over their territories. Though
functioning all these departments are not integrated in one unit with unified objectives andtasks, this network is not complex in full sense, so monitoring of many environmental
parameters is conducted by different offices and institutions independently without dueinteraction with each other.
Since 2004 through 2007 the IBPC SB RAS was performing research in the
Framework Programs of the joint academic council on life sciences on the project “Createa united network of complex ecological monitoring on biodiversity of frozen ecosystems
over the model territories of Yakutia boreal forests, tundra and forest-tundra”. By the
combined efforts of the institutes working in the system of the Yakut Science Center SB
RAS and participation of the foreign partnership serious investigations of the theoreticalprincipals of methodology and practice on ecological monitoring in Yakutia are carried out.
Monitoring on the state of rare and endangered animal and plant species is held, activity
related to their conservation and restoration in number are developed, more and more
remote aerospace techniques of research of the animal habitats, satellite location ofanimals during their migration are applied. Financial maintenance of the foreign
partnership contributes to setting up a network of field stations and polygons to perform
long-term studies of ecosystems’ state and development of the methods for optimizationof biological resources management in the national economy. Some field stations are
fitted with specific scientific equipment and devices and join in the World Network ofstations on ecological monitoring. On a monitoring network basis existed before andmainly owing to the previously implemented work realization of a real complex ecologicalmonitoring with collaboration of research institutes Siberian Branch RAS, other research
institutions of the Republic, Yakut State University, Ministry of Nature Protection andother interested bodies of Sakha is feasible. All data received will be used at theeconomical development of the region with consideration of strategy and tactics ofmanagement of the natural resources according to the National strategy of biologicaldiversity preservation in Russia.

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G5–P7㻔㻕㻔㻪㻘㻐㻳㻛
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G5–P9

CHEMICAL CHANGES AND FUNGAL COLONIZATION OF
SALIX ARCTICA LEAF AND STEM LITTER ON
DEGLACIATED MORAINES IN HIGH-ARCTIC CANADA
Takashi Osono1,*,

Dai Hirose2,

Masaki Uchida3,

Hiroshi Kanda31

Center for Ecological Research, Kyoto University, Shiga 520-2113 Japan

2

College of Pharmacy, Nihon University, Chiba 274-8555 Japan

3

National Institute of Polar Research, Tokyo 173-8515 Japan*tosono@ecology.kyoto-u.ac.jp
Relationships between chemical changes in decomposing leaf and stem
litter of Salix arctica and fungal colonization were examined in arctic tundra,
located within the proglacial field of the southern front of Arklio Glacier in the
Kreiger Mountains near Oobloyah Bay, Ellesmere Island, Nunavut, Canada.
Samples were collected in 2003 from five glacial moraines with different
development periods since the Last Glacial, the order of establishment of which isapparent based on the distance from the glacier snout and the moraines (Osono
et al. 2012). Samples of dead leaves and stems were divided into three and five
decay classes, respectively, using visual criteria and used for chemical analysis,
hyphal length estimation, and fungal isolation. Contents of acid unhydrolyzable
residues, extractives, and C varied significantly with the moraine and the decayclass of both leaves and stems. Contents of total carbohydrates, N, P, K, Ca, Mg,
C/N ratio, and δ15N varied significantly with either the moraine or decay class inleaves or stems. Total hyphal length ranged from 673 to 9470 m/g dry material inleaves and from 537 to 4404 m/g for stems and varied significantly with the decayclass in leaves and stems. Four morphotaxa were frequently isolated from leaves
and stems, and frequencies of occurrence of two morphotaxa varied significantlywith the decay class. Total hyphal length and frequencies of fungal morphotaxa
significantly correlated with contents of acid-unhydrolyzable residue, total
carbohydrates, extractives, N, P, K, Ca, Mg, C/N ratio, and/or δ15N in leaves andstems, suggesting organic chemical and nutritional controls on fungal
colonization.
_________________________________
Osono, T., Ueno, T., Uchida, M., Kanda, H., 2012. Abundance and diversity offungi in relation to chemical changes in arctic moss profiles. Polar Sci. 6, 121-131.

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G5–P10㻪㻘㻐㻳㻔㻓

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G5–P12ESTIMATION OF C LOSS BY FIRE IN A BURNED BLACKSPRUCE FOREST IN INTERIOR ALASKA USINGRADIOCARBON.
Miyuki Kondo1, Masao Uchida1, Yasuyuki Shibata1, Hiroki Iwata2,3, Yoshinobu
Harazono3,4
1

National Institute for Environmental Studies, Tsukuba, 305-8506, Japan

2

Graduate School of Agriculture, Kyoto University, Kyoto, 606-8502, Japan.

3International Arctic Research Center, University of Alaska Fairbanks, Fairbanks,

Alaska, 99775-7340,USA
4

Graduate School of Life and Environmental Sciences, Osaka Prefecture

University, Sakai, 599-8531, Japan
E-mail:kondo.miyuki@nies.go.jp

Carbon loss from forest floor/top soil by wildfire was estimated at a burned
boreal forest site in Interior Alaska, using radiocarbon (Δ14C). By comparingorganic C storage and radiocarbon profile at burned forest with those of a mature
forest, we estimated C loss from forest floor/top soil.

Soil profiles were surveyed

at the mature black spruce forest in University of Alaska Fairbanks, and theburned black spruce forest in Poker Flat Research Range, which burned in 2004
summer. The Δ14C profiles at the mature forest show clear bomb 14C peak after
1960’s, and plant litter and soil organic C at top of the 15cm was fixed over the
past 50 years.

Burned boreal forest site were similar Δ14C profiles to the mature

forest, but top of 10cm was lost. Organic carbon storage in each forest wasestimated by bulk density and C contents.

Decline of carbon storage after

wildfire was estimated, assuming that C storage in the mature forest were same
regime of C storage as burned stands before wildfire. Compare with mature forest,
4.4 kg C m-2 was lost. Wildfire disturbance in 2004 caused much C loss fromforest floor, corresponding to 53% of accumulated C over the past 50 years.

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Hiroshima University, Higashi-Hiroshima 739-8521, Japan
2
River Basin Research Center, Gifu University, Gifu 501-1193, Japan
3
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㻶㻘㻐㻳㻕Global methane simulation for the period 1910-2010 using
atmospheric general circulation model based chemistry transport
model
Arindam Ghosh1,2, Prabir K. Patra2, Kentaro Ishijima2, Shinji Morimoto1, Kenji
Kawamura1,3, Satoshi Sugawara4, Akihiko Ito5, Shuji Aoki6, and Takakiyo
Nakazawa6,2
1.
2.
3.
4.
5.
6.

National Institute for Polar Research, Tokyo, Japan
Research Institute for Global Change/JAMSTEC, Yokohama, Japan
Institute of Beogeosciences/JAMSTEC, Yokosuka, Japan
Miyagi Univ. of Education, Sendai, Japan
National Institute for Environmental Studies, Tsukuba, Japan
Center for Atmospheric and Oceanic Studies, Tohoku University, Sendai,JapanE-mail address of corresponding author: arindam@jamstec.go.jp

Methane (CH4) is produced both naturally and anthropogenically on the Earth’s
surface, and thought to be second only to carbon dioxide (CO2) as an agent ofpresent/future global warming. Methane is also chemically active, contributing toformation of tropospheric ozone and stratospheric water vapor, which further
increases its importance to the Earth’s radiative balance. Atmospheric CH4
concentration has increased from 900 ppb in 1900 to ~1800 ppb in 2000s [1]. During
the same period, the anthropogenic CH4 emission has increased from 92 Tg/yr toabout 310 Tg/yr. Mass balance calculation suggest that the increase in atmosphericconcentration is caused entirely due to increase in anthropogenic emissions [2].
Model simulations of atmospheric CH4 at monthly time scale with a horizontal
resolution of T42 spectral truncation (~2.8x2.8°) and 67 sigma-pressure verticallayers (surface - ~90 km), for ten different emission scenarios based on combinationsof anthropogenic (fossil fuel, biofuel, industrial process, livestock, waste handling andfire) and natural (wetland and rice) emission types, are being conducted using the
CCSR/NIES/FRCGC Atmospheric General Circulation Model (AGCM) based
Chemistry Transport Model (ACTM) for the period of 1900-2010. The model
simulations will be compared with CH4 concentrations as measured from the air
bubbles trapped in the polar ice columns, and direct measurements since the 1970s
at multiple sites around the globe.
Results on the contribution of different CH4 emission types to latitudinal and interannual/decadal variation of CH4 concentration over the past century will be
discussed.
References:[1] Etheridge, D.M., L.P. Steele, R.J. Francey, and R.L. Langenfelds. 1998.
Atmospheric methane between 1000 A.D. and present: evidence of anthropogenic
emissions and climatic variability. Journal of Geophysical Research, 103, 1597915996.
[2]
EDGAREmission
Databasefor
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S5–P3

 OCEANIC AND TERRESTRIAL BIOSPHERIC CO2UPTAKE ESTIMATED FROM ATMOSPHERIC POTENTIALOXYGEN OBSERVED AT NY-ÅLESUND, SVALBARD AND
SYOWA, ANTARCTICA
Shigeyuki Ishidoya1, Shinji Morimoto2, Shuji Aoki3, Shoichi Taguchi1, Daisuke
Goto3, Shohei Murayama1 and Takakiyo Nakazawa3
1

National Institute of Advanced Industrial Science and Technology (AIST),
Tsukuba 305-8569, Japan,23National Institute of Polar Research, Tokyo 190-8518, Japan,

Center for Atmospheric and Oceanic Studies, Tohoku University, Sendai
980-8578, Japan.
E-mail: s-ishidoya@aist.go.jp

Simultaneous measurements of the atmospheric O2/N2 ratio and CO2
concentration were made at Ny-Ålesund, Svalbard and Syowa, Antarctica for theperiod 2001-2009. Based on these measurements, the observed atmosphericpotential oxygen (APO) values were calculated. The APO variations produced bychanges in the oceanic heat content were estimated using an atmospherictransport model and heat-driven air-sea O2 (N2) fluxes, and then subtracted fromobserved interannual variations of APO. The oceanic CO2 uptake derived from theresulting “corrected” secular trend of APO showed interannual variability of lessthan ±0.6 GtC yr-1, significantly smaller than that derived from the “uncorrected”
trend of APO (±0.9 GtC yr-1). The average CO2 uptake during the period
2001-2009 was estimated to be 2.9±0.7 and 0.8±0.8 GtC yr-1 for the ocean andterrestrial biosphere, respectively. By excluding the influence of El Niño around2002-2003, the terrestrial biospheric CO2 uptake for the period 2004-2009
increased to 1.5±0.8 GtC yr-1, while the oceanic uptake decreased slightly to
2.8±0.7 GtC yr-1.

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TIME SERIES OF TROPOSPHERIC N2O ISOTOPOMERRATIOS OVER WESTERN SIBERIA
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Department of Environmental Science and Technology, 2Department of1

Environmental Chemistry and Engineering, Tokyo Institute of Technology, 4259
Nagatsuta, Midori-ku, Yokohama 226-8502, Japan
3

Research Institute for Global Change, Japan Agency for Marine-Earth Scienceand Technology, 3173-25 Showamachi, Kanazawa-ku, Yokohama 236-0001,
Japan
4

National Institute for Environmental Studies, 16-2 Onogawa, Tsukuba, 305-8506,

Japan
toyoda.s.aa@m.titech.ac.jp
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S5–P6

ANALYSIS OF INTER-ANNUAL VARIATIONS IN SEASONALCYCLE OF APO AT CAPE OCHI-ISHI<7RKMLPD+<DPDJLVKL+0XNDL70DFKLGDDQG&0LQHMLPD
1
National Institute for Environmental Studies, Tsukuba 308-8506, Japan
2
Tokyo University of Agriculture and Technology, 184-8588, Japan
E-mail: tohjima@nies.go.jp
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S5–P7

HIGH PRECISION CONTINUOUS MEASUREMENT SYSTEMFOR THE ATMOSPHERIC O2/N2 RATIO AT NY-ÅLESUND,SVALBARD
Daisuke Goto1, Shinji Morimoto2, Shigeyuki Ishidoya1, Shuji Aoki1 and Takakiyo
Nakazawa1
1: Center for Atmospheric and Oceanic Studies, Tohoku University, Sendai

980-8578, Japan2: National Institute of Polar Research, Tokyo190-8518, Japan

Contact address: d_goto@caos-a.geophys.tohoku.ac.jp
To elucidate temporal variations of atmospheric O2 at Ny-Ålesund (79˚N,
12˚E), Svalbard in detail, as well as to contribute to a better understanding of the
global carbon cycle, a high precision continuous measurement system for theatmospheric O2/N2 ratio was developed using a fuel cell oxygen analyzer. To
obtain highly precise values of the atmospheric O2/N2 ratio, pressure fluctuationsof the sample and standard air in the fuel cells were reduced to an order of 10−3
Pa, with temperatures stabilized to 32.0±0.1ºC. A non-dispersive infrared analyzer
was also installed into the system to allow simultaneous measurements of theatmospheric CO2 concentration. Considering remoteness of the observation site,
three special attentions were further paid when the measurement system wasconstructed; (1) the start-up and shutdown of the system can be controlled inJapan using the Internet, (2) all the output data from the system are recorded on ahard disk and also collected in Japan through the Internet, and (3) two water traps
were equipped in parallel on the air sample line to make it possible to operate thesystem over a long time without manually replacing the trap. The two traps arealternately switched to cool at −80ºC and heat at 50ºC in order to remove water
vapor contained in the sample air and the trap, respectively. By repeatedly
analyzing the same sample air, the analytical precision of the measurement
system was estimated to be ±1.4 per meg (0.3 ppm), which is sufficient for clearly
detecting very small spatiotemporal variations of the atmospheric O2/N2 ratio. We
also tested the system by continuously measuring the O2/N2 ratio in the boundary
layer atmosphere at Aobayama (38˚N, 141˚E), Sendai, Japan, and it was
confirmed that the system is capable of clearly detecting very small but persistentseasonal and diurnal cycles, along with short-term variations on time scales ofseveral hours to several days, caused by terrestrial biospheric and humanactivities. Systematic and continuous observation of the atmospheric O2/N2 ratiousing the developed system is planed to start at Ny-Ålesund in December 2012.

㻔㻖㻗㻶㻘㻐㻳㻛S5–P8

APPLICATION OF RADON-222 AS A TRACER FOR
CHARACTERIZING FETCH REGIONS AND EVALUATING A
GLOBAL 3D MODEL
Chunmao Zhu1, Hisayuki Yoshikawa-Inoue1, Hidekadzu Matsueda2, Yosuke Sawa2,
Yosuke Niwa2, Akira Wada3, Hiroshi Tanimoto4
1

Graduate School of Environmental Science, Hokkaido University, North 10 West 5,
North District, Sapporo 060-0810, Japan
2
Geochemical Research Division, Meteorological Research Institute, Nagamine 1-1,
Tsukuba 305-0052, Japan
3
Meteorological College, Asahi-cho, Kashiwa 277-0852, Japan
4
National Institute for Environmental Studies, 16-2 Onogawa, Tsukuba, Ibaraki 3058506, Japan
Corresponding author: Chunmao Zhu; E-mail: chmzhu@ees.hokudai.ac.jp
In order to estimate the regional/continental sources and sinks for atmosphericCO2, atmospheric Radon-222 has been used at Rishiri Island (45°07’N, 141°12’E)
as a tracer being monitored since December 2008. This work analyzed the first two
years atmospheric Radon-222 data to evaluate the seasonal transport pattern. In
summer, clear diurnal variation was observed with maximum Radon-222
concentration before the dawn, while the minimum appeared in the afternoon. Thiswas caused by the local radon-222 source. However the magnitude of local source
was quite weak. Seasonal Radon-222 variation was characterized by highconcentrations from November to February and low concentrations from May to
July, caused by the alternation of continental and maritime fetch regions. Seasonalhigh and low Radon-222 events were examined by using the back trajectory cluster
analyses to clarify the fetch regions (Fig.
1). The results indicated that the
predominant continental fetch region was
southeastern Siberia and northeastern
China. Radon-222 emitted from China andSouth Korea, whose economies are
growing rapidly, did not significantly affect
the Rishiri site. This implies that current
observation of CO2 at Rishiri Island ismore directly influenced by the carbon
sink region vegetated by boreal forest.
The major maritime fetch region was the
Sea of Okhotsk and the Bering Sea. A
global three-dimensional model (NICAMTM) accurately simulated Radon-222
concentrations on Rishiri Island and in theseasonal fetch regions. Other than toevaluate the sources of atmosphericgreenhouse gases being monitored at
Rishiri Island, the time series of RadonFig. 1. Fetch regions for high and low radon-222
222 data will also allow us to validate
events at RIO as indicated by 120-h back trajectorymodel simulations used to examine
clusters. The values near each trajectory show thetrans-boundary air pollution.
ratio of events contributing to that cluster relative tototal events in the specified season.

㻔㻖㻘㻶㻘㻐㻳㻜
S5–P9

RECONSTRUCTION OF PAST VARIATIONS OF THE
CARBON AND HYDROGEN ISOTOPIC RATIOS IN
ATMOSPHERICMETHANEFROMITSVERTICAL
DISTRIBUTION OBSERVED IN NGRIP FIRN
Satoshi Sugawara1, Taku Umezawa2, Kenji Kawamura3, Shinji Morimoto3,
Shuji Aoki4 and Takakiyo Nakazawa4
1

Institute of Earth Science, Miyagi University of Education, Sendai, Japan
Max Planck Institute for Chemistry, Mainz, Germany3
National Institute of Polar Research, Tokyo, Japan
4
Center for Atmospheric and Oceanic Studies, Tohoku University, Sendai, Japan(sugawara@staff.miyakyo-u.ac.jp)
2

Temporal variations of δ13C and δD of atmospheric CH4 in the past 50 years werereconstructed from the isotopic ratios of CH4 observed in firn at North GRIP. The
one-dimensional diffusion model was used to simulate the diffusion process andthe gravitational separation of CH4 molecule in the firn. The effective diffusivity
was determined so that the difference between the modeled and observed CO2
concentration profiles was minimized. An approximate history of the atmosphericCH4 concentration was constructed for NGRIP by combining the data from thedirect atmospheric measurements at Point Barrow, Alert, and Ny-Ålesund withthose from ice cores at Greenland. In order to reconstruct the past δ13C and δDof atmospheric CH4 from their values in the firn, the effective age of CH4 at eachsampling depth was determined by using an approximate history of theatmospheric CH4 concentration. Effective age at each sampling depth was
determined so that the model-calculated concentration at that depth agreed with avalue in the concentration history. To correct for the diffusion effect on δ13C of CH4
in the firn, the diffusion model was run without the gravitational effect, using
concentration histories for three kinds of CH4 molecules, 12CH4 with D16, 13CH4
with D17, and 13CH4 with D16. Here, D16 and D17 represent the effective diffusivities
of CH4 molecules with masses 16 and 17, respectively. The diffusion correction
was determined as a difference between the isotopic value of the heavier
molecule actually predicted in the firn (δ13C(D17)) and the value which theoretically
excluded the effect of diffusive separation (δ13C(D16)). Correction for the diffusion
effect on δD was the same as that of δ13C, but used three molecules of CH4 with
D16, CH3D with D17 and CH3D with D16. The values of the atmospheric δ13C, thus
estimated, were in good agreement with those from direct atmosphericmeasurements at Ny-Ålesund. The statistical uncertainty of the reconstruction
procedure was examined by repeating model calculation with 100 different data
sets provided by adding normal pseudo random numbers to the observed values
in firn. We will also discuss an application of the diffusion correction to the isotopic
values of CH4 observed by ice core analyses.

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Arctic Data archive System (ADS)
Hironori Yabuki1,2,

Haruko Kawamoro1

1 Arctic Environment Research Center (AERC), National Institute of Polar
Research (NIPR),Tachikawa-shi, Tokyo, 190-8518 JAPAN2 Research Institute for Global Change(RIGC), Japan Agency for Marine-Earth
Science and Technology (JAMSTEC) Yokosuka, 237-0061, JAPANE-mail: yabuki@jamstec.go.jp
In Arctic region, various changes are being caused by global warming. In
previous studies, the decrease of Arctic sea ice extent, the increase in soil
temperature in the region of Siberia, permafrost melting, the increase in Arctic
river runoff, reduction in snow cover has been revealed. Also the impact of humanactivities and ecosystems due to these changes is concerned. The actual
condition and mechanism of environmental change in arctic has not been
elucidated. Previous studies have been carried out to separate the atmosphere,
oceans, by land. Arctic is a system consisting of atmosphere, ocean, land surface,from snow and ice, these systems including the phenomenon of different spatial
scales and time scale, respectively. In order to clarify the variability of the Arctic
environment, through interdisciplinary research, research is needed in using a
database that integrates the results of observation and research data acrossmultiple areas.
On the other hand, arctic research by Japanese researchers has been
carried out all the time from the last century. The result of their research includes
many irreplaceable data, such as observation time series, sample, and its
analysis, which each researcher got in the field. Since researcher andorganization have had those data in their keeping by their way, many data has not
managed and kept systematically.
Now, a new ‘Arctic Data archive System (ADS)’ was launched on purpose
to collect, manage and open some arctic data supported by Green Network of
Excellence (GRENE), Rapid Change of the Arctic Climate System and its Global
Influences (a tentative English title). ADS can search various keywords using
metadata which are related with a one-to-one correspondence. This schema fitssome format of typical Earth environment data, and we plan additional schema.

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S5–P15OVERVIEW OF REGIONAL AND INTERANNUAL
VARIATIONS OF SNOW AND SURFACE CONDITIONS AT
GRENE ARCTIC OBSERVATION SITES DERIVED BYSATELLITE MICROWAVE DATA1XHUDVLPXJXOL$OLPDVL+LUR\XNL(QRPRWR6KXKHL7DNDKDVKL
1

Kitami Institute of Technology, 165 Koen-cho, Kitami, Hokaido, Japan

2

National Institute of Polar Research, 10-3 Tachikawa, Tokyo, Japan

E-mail address of corresponding author: dse10841@std.kitami-it.ac.jp
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S5–P16

JAPANESE FIELD ACTIVITIES IN THE GREENLAND ICESHEET MONITORING NETWORK (GLISN)*HQWL7R\RNXQL0DVDNL.DQDR<RNR7RQR7HWVXWR+LPHQR6HLML7VXERL
1

Tohoku University, 6-6 Aza-Aoba, Aramaki, Aoba-ku, Sendai 980-8578, Japan

2

NIPR, 10-3, Midoricho, Tachikawa, Tokyo 190-8518, Japan

3

JAMSTEC, 3173-25, Showa-machi, Kanazawa-ku, Yokohama 236-0001, Japan

4

Seikei University, 3-3-1 Kichijoji-Kitamachi, Musashino, Tokyo 180-8633, Japan

toyokuni@aob.gp.tohoku.ac.jp
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S5–P17

GLACIOLOGICAL OBSERVATIONS IN SUNTAR-KHAYATARANGE, EASTERN SIBERIA, 2012
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1

Kitami Institute of Technology, 165 Koen-cho, Kitami, Hokkaido 090-8507, Japan

2

Japan Agency for Marine-Earth Science and Technology, 3173-25, Showa-machi,

Kanazawa-ku, Yokohama-city, Kanagawa 236-0001, Japan
3

Chiba University, 1-33, Yayoi-cho, Inage-ku, Chiba-shi, Chiba 263-8522, Japan

4

National Institute of Polar Research, 10-3, Midoricho, Tachikawa, Tokyo

190-8518, Japan
5

Melnikov Permafrost Institute, 677010, Yakutsk, 36, Merzlotnaya str. MPI SB

RussiaCorresponding author: Tatsuo Shirakawa, shirakaw@mail.kitami-it.ac.jp
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S5–P22SEA-ICE THICKNESS CHARACTERISTICS REVEALED BY
OBSERVATIONS IN THE CANADA BASIN
J. Ono1,2,

K. Tateyama3,

D. Hirano1,4,

A. Orlich5

1

National Institute of Polar Research, Tokyo, Japan

2

The University of Tokyo, Chiba, Japan

3

Kitami Institute of Technology, Hokkaido, Japan

4

Tokyo University of Marine Science and Technology, Tokyo, Japan

5

University of Alaska Fairbanks, Alaska, USA

E-mail: jo@1.k.u-tokyo.ac.jp
To observe ocean and sea ice conditions in the Canada Basin of the Arctic
Ocean, a scientific cruise of the Canadian Coast Guard Ship Louis S. St-Laurent
was conducted from 2 August to 8 September 2012. Using an electromagnetic
induction instrument (EM) along with Passive Microwave Radiometers (PMR),
underway measurements of sea-ice thickness were carried out on August 8 to 10(offshore of Barrow) and 27 to 29 (around 80oN). Sea-ice thicknesses measured
by the EM spatially changed with the range of 0.1-3.0 m. To reveal sea-ice
thickness distribution in more detail, probability density was examined. Although
the modal sea-ice thickness existed in 0-0.1 m, the probability density was higher
around 80oN than offshore of Barrow. Measurements of sea-ice thickness with aportable EM were also done along four transect lines at two ice stations (80.88oN,
137.41oW and 80.21oN, 129.97oW) on August 26 and 27. The mean sea-ice
thicknesses for each transect lines were 1.35, 1.34, 0.38, and 2.46 m, respectively.
From the entire data, the maximum (minimum) sea-ice thickness was 2.52 (0.26)
m. Sea-ice thicknesses obtained from the EM agree fairly well with those basedon the drill-hole measurements. The correlation coefficient between them was
0.96. In addition to the detailed discussion, results obtained from PMR andrelationship between sea ice and ocean conditions will be introduced during thepresentation of the day.

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0.05
heat transport [PW]

R=−0.72

0

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2100

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2300

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years

2500

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Visible Remote Sensing Information for Snow Monitoring
Igor Appe,IMSG/NOAA

iappel@earthlink.net
The launch of advanced instruments onboard of new operational and research satellites
greatly improves the potential of mapping and monitoring snow cover. Increasing spectral
coverage of the data and frequency of observations allows for more accurate snow coverdetection and timely identification of changes in the snow pack properties. A higher spatial
resolution of satellite observations provides better opportunity for a much more detailed
characterization of the snow cover distribution needed for various applications. As a resultof the advancement in remote sensing, the information on snow cover from satellites isbeing increasingly used not only in global and continental-scale studies but also in regional
and local scale investigations. Snow monitoring to a great degree depends on using visible
channels even though such data of satellite observations could have significant gaps.
The advance in snow remote sensing is accompanied by increasing requirements tosnow products – resolution finer than 1 km, snow fraction in addition to snow extent, awider range of snow properties. To meet those growing requirements, improved retrieval
algorithms and snow models should be developed for visible spectral bands.
A promising direction to create automatic snow retrievals of improved quality isdeveloped by the author of the presentation and implemented in several algorithms. The
algorithms were accepted to retrieve all the Visible Infrared Radiometer Suite (VIIRS)
snow products in NOAA and have been successfully used to routinely generate daily global
maps of snow cover fraction from the Moderate Resolution Imaging Spectroradiometer(MODIS) at GSFC/NASA.
Proper validation is a critically important means to develop snow cover retrieval. Daily
snow depth data acquired from more than 1000 World Meteorological Organization(WMO) stations and approximately 1500 US Cooperative stations are currently used toestimate the accuracy of snow derivation from daily VIIRS observations. Another method
implemented to analyze the performance of snow algorithms utilizes high-resolution
observations as an effective source of ground truth information for snow fraction.
To further improve processing of satellite observations on snow, the strategy
characterized by the following distinguishing features is currently under development.
Creating snow algorithms, first of all, it is proposed to derive scene-specific (or evenpixel-specific) parameters characterizing local properties of snow and non-snow
endmembers. The application of such approach requires adjustment of algorithms tovarying regional conditions.
Another opportunity to improve snow retrieval is related to the use of snow BRDF
models. It has been demonstrated that the means of geometric optics could reliably describe
angular dependencies related to bidirectional snow reflectance, and a simple asymptotic
analytical model could be used to calculate bidirectional reflectance. Possible applicationsof the asymptotic analytical BRDF model for remote sensing include sensor calibration,
calculating snow albedo, normalizing reflectances, and retrieval of snow grain size needed,in particular, for microwave observations on snow.
The combination of scene-specific algorithms with analytical BRDF model and synergyof remote sensing retrieval algorithms with conventional observations will help create
unbiased and consistent information on snow cover.

㻕㻖㻗S4-O13
THE INTIERNATIONAL STUDY OF ARCTIC CHANGE:PROVIDING TIMELY, RELEVANT AND ACCESSIBLESCIENTIFIC INFORMATION FOR RESPONDING TO ARCTIC
CHANGEPeter Schlosser1,
1

Maribeth Murray2,

Lize-Marié van der Watt3

The Earth Institute, Columbia University, 405 Low Library, MC 4335 535, West116th Street, New York, NY 10027, United States of America.
2

International Arctic Research Center, (International Study of Arctic Change)

University of Alaska Fairbanks, PO 757340 Fairbanks, Alaska 99775, UnitedStates of America.
3

International Study of Arctic Change, Polarforskningssekretariatet, Box 50003

104 05 Stockholm, Sweden.
schlosser@ldeo.columbia.edu
The International Study of Arctic Change is an internationally supported
program of arctic environmental change research with the overall objective ofproviding timely, relevant and accessible information for responding to rapid arctic
change. ISAC works to enable the research community to transcend national
limitations and to enhance arctic research within an international framework.
Recent and continuing changes across all components of the Arctic System arehaving significant impacts on the natural, the human, and the built environment;
and these changes are influencing domestic policies and international relations.
Future system states are uncertain and the lack of predictability hinders efforts todevelop strategies for adapting to and managing a changing Arctic. ISAC provides
an overarching framework to integrate diverse programs and projects with thecommongoals

ofobserving,understanding

andresponding

toarcticenvironmental change. The ISAC Science Plan provides a vision for integrating
research among diverse fields and varied users and stakeholders. This paper
focusses the implementation of ISAC, including responding to change initiatives
and the inaugural 2013 Arctic Observing Summit, which aims to provide
community-driven, science-based guidance for the design, implementation,
coordination and sustained long-term (decades) operation of an international
network of arctic observing systems within the framework of the Sustaining Arctic
Observing Networks (SAON) initiative.

G7-P8
Toward Hierarchical Modeling and Prediction of the Arctic
Climate System
Wieslaw Maslowski, Jaclyn Clement Kinney, Andrew Roberts, Anthony Craig Naval Postgraduate School, Monterey CA, USA
Robert Osinski - Institute of Oceanology Polish Academy of Sciences,
Sopot, Poland
John J. Cassano - University of Colorado, Boulder, CO, USA
William J. Gutowski - Iowa State University, Ames. IA, USA
Bart Nijssen, Dennis P. Lettenmaier - University of Washington, Seattle, WA, USA
William H. Lipscomb - Los Alamos National Laboratory, Los Alamos, NM, USA
Slawek M. Tulaczyk - University of California, Santa Cruz, CA, USA
Xubin Zeng - University of Arizona, Tucson, AZ, USA

Arctic sea ice is a key indicator of the state of global climate because of both its
sensitivity to warming and its role in amplifying climate change.
Accelerated melting of the perennial sea ice cover has occurred since the late 1990s,
which is important to the pan-Arctic region, through effects on atmospheric and oceanic
circulations, the Greenland ice sheet, snow cover,permafrost, and vegetation as well as it affects the global surface energy and moisturebudgets, atmospheric and geosphere-biosphere feedbacks.
We evaluate available results from CMIP5 models against limited observations for theirskill in representing recent decadal variability of Arctic sea ice area, thickness, drift andexport. We also intercompare results from CMIP5 models with selected CMIP3 models
and a hierarchy of regional ice-ocean and fully coupled climate models to demonstratepossible gains or outstanding limitations in representing physical processes of potential
importance to past and present climate variability in the Arctic. We argue that the limited
ability of global models to realistically reproduce some of the critical processes affecting
recent warming and sea ice melt in the Arctic Ocean distorts predictability of EaSMs andlimits the accuracy of their future arctic and global climate predictions. To better
understand the past and present states and estimate future trajectories of Arctic sea ice
and climate, we argue that it is critical to advance hierarchical arctic regional climate
modeling and coordinate it with the design of an integrated Arctic observing system toconstrain models.