9th Biennial Workshop on Japan-Kamchatka-Alaska
Subduction Processes (JKASP 2016)

Understanding active subduction processes in North Pacific arcs

MAY 31 – JUNE 3, 2016
SCIENTIFIC PROGRAM &ABSTRACTSGEOPHYSICAL INSTITUTE
UNIVERSITY OF ALASKA FAIRBANKSFAIRBANKS, ALASKA

1

Conference Sponsors
Geophysical Institute, University of Alaska Fairbanks
College of Natural Science and Mathematics, University of Alaska Fairbanks
Local Organizing Committee
Jeff Freymueller, Geophysical Institute, University of Alaska Fairbanks
Pavel Izbekov, Geophysical Institute, University of Alaska Fairbanks
John Eichelberger, Graduate School, University of Alaska Fairbanks
Cheryl Cameron, Alaska Division of Geological & Geophysical Surveys
Michelle Coombs, Alaska Volcano Observatory, USGSDavid Fee, Geophysical Institute, University of Alaska Fairbanks
Taryn Lopez, Geophysical Institute, University of Alaska Fairbanks
Jessica Larsen, Geophysical Institute, University of Alaska Fairbanks
Dmitry Nicolsky, Geophysical Institute, University of Alaska Fairbanks
John Power, Alaska Volcano Observatory, USGS
Natalia Ruppert, Geophysical Institute, University of Alaska Fairbanks
Janet Schaefer, Alaska Division of Geological & Geophysical Surveys
Elena Suleimani, Geophysical Institute, University of Alaska Fairbanks
Kristi Wallace, Alaska Volcano Observatory, USGSPeter Webley, Geophysical Institute, University of Alaska Fairbanks
Michael West, Geophysical Institute, University of Alaska Fairbanks
Technical Support*
Lea Gardine (logistics)
Kimberly Cummins (visa support)* all at the Geophysical Institute, University of Alaska Fairbanks

2

TABLE OF CONTENTS

Page

SCIENTIFIC PROGRAM ……………………………………………………………………………….. 4
MONDAY, MAY 30 ……………………………………………………………………………….. 4
TUESDAY, MAY 31 ……………………………………………………………………………….. 4
WEDNESDAY, JUNE 1 …………………………………………………………………………… 6
THURSDAY, JUNE 2 ………………………………………………………………………………. 9
FRIDAY, JUNE 3 …………………………………………………………………………………….. 10
ABSTRACTS ………………………………………………………………………………………………… 12
Keynote Talk …………………………………………………………………………………………. 12
Seismology (Oral presentations) …………………………………………………………… 16
Tectonics and Experiments (Oral presentations)..………………………………….. 31
Geology & Petrology & Geochemistry (Oral presentations) …………………… 38
Interdisciplinary Poster Session …………………………………………………………….. 56
Volcano Monitoring (Oral presentations) ……………………………………………… 97
Tsunami (Oral presentations) ……………………………………………………………….. 114
AUTHORS INDEX ……………………………………………………………………………………….. 117

3

SCIENTIFIC PROGRAM
MONDAY, MAY 30
On-site registration and ice-breaker

IARC lobby, 16:00-19:00

Hosts: Jeff Freymueller and Pavel Izbekov; registration: Lea Gardine
16:00
Registration opens
17:00
Ice-breaker starts
TUESDAY, MAY 31
On-site registration and morning coffee
07:00
07:30

REIC lobby, 07:00 – 08:00

On-site registration continues
Breakfast
PLENARY SESSION

Welcoming remarks
08:00
08:10
08:20

REIC 201, 08:00 – 08:40

Introduction: Jeff Freymueller
Welcome: Robert McCoy, Director of the Geophysical InstituteWelcoming remarks from John Eichelberger (UAF), Evgenii Gordeev (Institute ofVolcanology and Seismology), and Minoru Kasahara (Hokkaido University)

Keynote Talk
08:40

REIC 201, 08:40 – 09:00

David W. Scholl, Stephen H. Kirby, and Roland Von Huene BASED ON GLOBALOBSERVATIONS, TWO REASONS WHY THE ALEUTIAN-ALASKA SUBDUCTION ZONEIS PRONE TO RUPTURE IN GREAT (> Mw8.0) MEGATHRUST EARTHQUAKESTECHNICAL SESSIONS

Seismology (Oral presentations)

REIC 201, 09:00 – 10:00

Chairs: Mike West and Matt Haney
09:00
Stephen R. McNutt, Glenn Thompson, Jochen Braunmiller, and Stephen Holtkamp
PEAK RATES AND LARGEST MAGNITUDE EVENTS IN EARTHQUAKE SWARMSFROM DIFFERENT TECTONIC SETTINGS
09:20
Hiroaki Takahashi, Mako Ohzono, Koji Minato, Noritoshi Okazaki, Takahiro Suzuki,
Tetsuya Takahashi, Fujio Akita MAGMA, THERMAL STRUCTURE, STRAIN
CONCENTRATION AND ACTIVE SEISMICITY IN KUSSHARO CALDERA, HOKKADIO,JAPAN4

09:40

Nikolai Shapiro, Dmitry Droznin, Svetlana Droznina, Victor Chebrov, Evgeny
Gordeev, William Frank THE REVEALING OF THE VOLCANIC ACTIVITY FORKLYUCHEVSKAYA GROUP OF VOLCANOES FROM CONTINUOUS SEISMIC RECORDS

10:00

Coffee break

Seismology (Oral presentations), continued

REIC 201, 10:20 – 12:00

Chairs: Hiroaki Takahashi and John Lyons
10:20
Alexandra K. Farrell and Stephen R. McNutt SEISMIC ATTENUATION, TIME DELAYSAND RAYPATH BENDING OF TELESEISMS BENEATH CERRO UTURUNCU, BOLIVIA
10:40
Matthew M. Haney, Victor C. Tsai, Kevin M. Ward WIDESPREAD IMAGING OF THE
LOWER CRUST, MOHO, AND UPPER MANTLE BENEATH ALASKA FROM RAYLEIGH
WAVES
11:00
Stephen Holtkamp USING EARTHQUAKES TO PROBE SUBDUCTION MEGATHRUSTBEHAVIOR: A LOOK AT EARTHQUAKE SWARMS AND REPEATING EARTHQUAKESIN ALASKA
11:20
Anna Skorkina, Alexander Gusev CORNER FREQUENCIES OF SOURCE SPECTRA OF
MODERATE SUBDUCTION-ZONE EARTHQUAKES OBSERVED NEAR THE AVACHA
BAY, KAMCHATKA
12:00

Lunch

Seismology (Oral presentations), continued

REIC 201, 13:00 – 14:40

Chairs: John Power and Hiroaki Takahashi
13:00
Mako Ohzono, Hiroaki Takahashi, Nikolay V. Shestakov, Guojie Meng, Mikhail. D.
Gerasimenko ESTIMATION OF THE LONG-TERM EFFECT OF VISCOELASTICRELAXATION INDUCED BY THE 2011 TOHOKU EARTHQUAKE AND OTHER
INTERPLATE EARTHQUAKES AROUND NORTHEASTERN ASIA
13:20
John J. Lyons, Matthew M. Haney, Cynthia Werner, Peter Kelly, Matthew Patrick,Christoph Kern, and Frank Trusdell LONG PERIOD SEISMICITY AND VERY LONGPERIOD INFRASOUND DRIVEN BY SHALLOW MAGMATIC DEGASSING AT MOUNTPAGAN, MARIANA ISLANDS
13:40
Matthew M. Haney, Robin Matoza, David Fee, David F. Aldridge SEISMIC
EQUIVALENTS OF INFRASONIC SCALING LAWS FOR VOLCANIC JETS AND
ACOUSTIC MULTIPOLES
14:00
Cassandra M. Smith, Stephen R. McNutt, Glenn Thompson QUANTIFYINGGROUND COUPLED AIR WAVES TO DETERMINE GAS FLUX AT PAVLOF VOLCANO,ALASKA, DURING THE 2007 ERUPTION
14:20
Michael West, Matt Gardine, Natalia Ruppert, Carl Tape, Jeffrey Freymueller,
Stephen Holtkamp PERSPECTIVES ON THE MW7.1 INISKIN EARTHQUAKE
14:40
Coffee break5Tectonics and experiments (Oral presentations)

REIC 201, 15:00 – 16:20

Chair: Jeff Freymueller
15:00
Jeff Freymueller PLATE BOUNDARIES IN THE NORTH PACIFIC
15:20
Higashi Uchida STRAINMETER ARRAY OBSERVATION OF THE DIKE INTRUSION AT
SAKURAJIMA VOLCANO ON 15 AUGUST 2015
15:40
Johan Gilchrist and Mark Jellinek SEDIMENT WAVES AND CLOUD LAYERING IN
EXPLOSIVE VOLCANIC ERUPTIONS: EVIDENCE FROM ANALOGUE EXPERIMENTS
16:00
Shanshan Li, Jeff Freymueller, Natalia Ruppert, Jianjun Wang CORRELATIONSTUDY OF COULOMB STRESS CHANGE IMPARTED BY TWO NEW SLOW SLIPEVENTS AND SEISMIC RATE CHANGE IN LOWER COOK INLET OF THE ALASKAALEUTIAN SUBDUCTION ZONEWEDNESDAY, JUNE 1
Morning coffee and informal discussions
07:30

REIC lobby, 07:30 – 08:00

Breakfast.
TECHNICAL SESSIONS

Geology & Petrology & Geochemistry (Oral presentations)

REIC 201, 08:00 – 10:00

Chairs: Michelle Coombs and Kirsten Nicolaysen
08:00
Izumi Yokoyama ORIGIN OF CALDERAS: COLLAPSES OR EXPLOSIONS?
08:20
Maxim Portnyagin, Kaj Hoernle, Reinhard Werner, Boris Baranov, Gene
Yogodzinski and BERING participants BERING - A NEW INTERNATIONAL MARINERESEARCH PROJECT TO INVESTIGATE THE MAGMATIC AND TECTONIC EVOLUTION
OF THE BERING SEA AND ITS MARGINS
08:40
Kirsten Nicolaysen, Dixie West, Virginia Hatfield, Breanyn MacInnes, Mitsuru
Okuno, Arkady Savinetsky, Olga Krylovich, Pavel Izbekov, Lyman Persico, John
Lyons, Max Kaufman, Christina Neal, William E. Scott, John Power A CASE FORINTEGRATED GEOSCIENCE AND ARCHEOLOGICAL STUDIES IN THE ALEUTIAN ARC
09:00
Owen K. Neill, Christopher J. Nye EVIDENCE FOR MAGMA MIXING AND RAPIDMAGMATIC ASCENT IN GROUNDMASS GLASS COMPOSITIONS FROM THE 2008
ERUPTION OF KASATOCHI, CENTRAL ALEUTIAN ISLANDS
09:20
Taryn Lopez, Tobias Fischer, Andrea Rizzo ISOTOPIC CONSTRAINTS ON VOLATILECYCLING WITHIN THE ALEUTIAN ARC
09:40
Alex M. Iezzi, Douglas M. Thompson, Beverly Chomiak LAHAR INUNDATIONMODELING WITH THE AID OF HISTORIC FLOW DEPOSITS AT REDOUBT VOLCANO,COOK INLET, ALASKA
10:00

Coffee break6

Geology & Petrology & Geochemistry (Oral presentations)cont. Taryn Lopez and Pavel Izbekov
Chairs:
10:20
10:40

11:00

11:20

11:40

12:00

Michelle Coombs and Brian Jicha GEOLOGY AND 40AR/39AR GEOCHRONOLOGY OF
LONG-LIVED AKUTAN VOLCANO, EASTERN ALEUTIAN ISLANDS
Daniel Rasmussen, Terry Plank, Amanda Lough, Pete Stelling, Diana RomanPETROLOGIC CHRONOLOGY OF THE 1999 SUB-PLINIAN ERUPTION OF SHISHALDIN
VOLCANOSam H. Sheffer, Virginia Hatfield, Kirsten Nicolaysen, Thomas Bartlett III, Dixie
West, Emily Deacon, Kale Bruner SOURCING PREHISTORIC OBSIDIAN TOOLS IN
THE ISLANDS OF FOUR MOUNTAINS, ALASKA
Alexander Proussevitch, Pavel Izbekov, Dork Sahagian THE RELATION BETWEEN
PRE- FRAGMENTATION BUBBLE SIZE DISTRIBUTION, ASH PARTICLE
MORPHOLOGY, AND THEIR INTERNAL DENSITY: IMPLICATIONS TO VOLCANIC ASH
TRANSPORT AND DISPERSION MODELS
O.V. Bergal-Kuvikas, V.L. Leonov, A.N. Rogozin, I.N. Bindeman, E.S. Kliapitskiy
NEW DISCOVERED LATE MIOCENE VERCHNEAVACHINSKAY CALDERA ON EASTERNKAMCHATKA (UPSTREAM OF LEVAYA AVACHA AND KAVYCHA RIVERS): GEOLOGY,
BOUNDARY AND COMPOSITION
Lunch

Geology & Petrology & Geochemistry (Oral presentations)cont. Taryn Lopez and Pavel Izbekov
Chairs:
13:00
13:20

REIC 201, 10:00 – 12:00

REIC 201, 13:00 – 13:40

Cheryl Cameron, Katherine Mulliken, Janet Schaefer, Kristi Wallace, Scott Crass
ALASKA TEPHRA DATABASE
Jessica F. Larsen, Janet R. Schaefer, James W. Vallance PETROLOGY AND
GEOCHEMISTRY OF THREE EARLY HOLOCENE ERUPTIONS FROM MAKUSHIN
VOLCANO, ALASKAInterdisciplinary poster session

REIC lobby, 14:40 – 17:00

Presiding: Jeff Freymueller and Pavel Izbekov
Coffee will be served at 14:40.
1
Celso R. Alvizuri and Carl Tape FULL MOMENT TENSOR AND SOURCE-TYPE ESTIMATIONFOR VOLCANIC EVENTS
2Ophelia George, Joan L. Latchman, Charles Connor, Stephen McNutt, Laura Connor
GENERATING DYNAMIC VOLCANIC HAZARD MAPS FOR DOMINICA, LESSER ANTILLES BY
USING GEOPHYSICAL DATA AS WEIGHTS IN SPATIAL INTENSITY MAPS
3
A.V. Kiryukhin, S.A. Fedotov, P.A. Kiryukhin GEOMECHANICAL INTERPRETATION OF LOCALSEISMICITY CONCERNING ACTIVITY OF TOLBACHIK, KORYAKSKY AND AVACHINSKY
VOLCANOES OF KAMCHATKA IN 2008-2012
7

4
5
6

7

8
9

10

11

12

13

14

15

16

Vipul Silwal and Carl Tape SEISMIC MOMENT TENSORS AND ESTIMATED UNCERTAINTIES IN
SOUTHERN ALASKA SUBDUCTION ZONE
Michael West, Natalia Ruppert, Natalia Kozyreva, Sara Meyer, Dara Merz, Miriam Braun
TRACKING GLACIERS WITH THE ALASKA SEISMIC NETWORK
Yusuke Yamashita, Masanao Shinohara, Tomoaki Yamada, Kazuo Nakahigashi , Hajime
Shiobara, Kimihiro Mochizuki, Takuto Maeda, Kazushige Obara LONG-TERM OCEAN
BOTTOM MONITORING OF SLOW EARTHQUAKES ON THE SHALLOW PLATE INTERFACE IN
HYUGA-NADA, WESTERN PART OF THE NANKAI TROUGH
Noritoshi Okazaki, Ryo Takahashi, Makoto Tamura, Hiroaki Takahashi, Masayoshi
Ichiyanagi, Teruhiro Yamaguchi, Ryo Honda, Yosuke Miyagi, Akimichi Takagi GRAVITYDECREASE AND VOLCANIC INFLATION AROUND THE ACTIVE CRATER AT TOKACHI-DAKE
VOLCANO, HOKKAIDO, JAPAN
S.S. Serovetnikov, E.I. Gordeev, Hiroaki Takahashi, Pavel Izbekov THE KLUCHEVSKAYAVOLCANO GROUP OBSERVATION NETWORK 2006-2016. RUSSIA, KAMCHATKA.
Nikolay Shestakov, Grigory Nechaev, Nikolay Titkov, Mikhail Gerasimenko, Victor Bykov,
Victor Pupatenko, Sergey Serovetnikov, Alexander Prytkov, Nikolay Vasilenko, Dmitry
Sysoev, Alexey Sorokin, Hiroaki Takahashi and Mako Ohzono HAVE THE POSTSEISMIC
MOTIONS DUE TO THE MAY 24, 2013 Mw 8.3 OKHOTSK DEEP FOCUS EARTHQUAKE BEEN
DISCOVERED BY THE RUSSIAN FAR EAST GNSS NETWORKS?
Natalia Gorbach, Maxim Portnyagin, Tatiana Philosofova COMPOSITIONAL TRENDS OFАMPHIBOLE IN 2001-2013 YOUNG SHIVELUCH ANDESITES AS EVIDENCE OF MAGMACHAMBER REPLENISHMENT AND SUBSEQUENT CONVECTION
Natalia Gorbach, Anastasiya Plechova , Dmitry Melnikov and Sergey Samoilenko LANDSLIDEAT ZНUPANOVSKY VOLCANO (KAMCHATKA) IN JULY 2015: DISTRIBUTION OF THE DEPOSITSAND POTENTIAL PRECURSORS
Kosuke Ishige, Mitsuhiro Nakagawa, Seiko Yamasaki, Akikazu Matsumoto GEOLOGY ANDPETROLOGY OF TAISETSU VOLCANO GROUP, JAPAN; EVOLUTION OF MAGMA AND
ACTIVITY AGES.
Olga Khubaeva and Antonina Nikolaeva THERMAL SUPPLY OF HYDROTHERMAL SYSTEM, A
CASE STUDY OF THE BOGDANOVICH VOLCANIC CENTER HYDROTHERMAL SYSTEM(PARAMUSHIR ISLAND, THE KURIL ISLANDS)
Olga Khubaeva, Pavel Izbekov, Sergey Samoylenko, and John Eichelberger MUTNOVSKYAND GORELY VOLCANOES IN KAMCHATKA: A PERFECT CLASSROOM FOR TEACHING
VOLCANOLOGY
Heather Miller, Jake Roush, Taryn Lopez, Tobias Fischer, Matt Schrenk FIRE AND LIFE:
MICROBIAL MEDIATION OF DEEP CARBON CYCLING ALONG THE “RING OF FIRE”, A
SUBDUCTING OCEANIC LITHOSPHERE, WESTERN ALEUTIAN ISLANDS
Mitsuhiro Nakagawa THE EFFECT OF THE AD 1611SANRIKU EARTHQUAKE ON VOLCANIC
ACTIVITY IN HOKKAIDO, JAPAN

8

17

18
19

20

21
22

23

24

25

26

27

A.G. Nikolaeva, G.A. Karpov, A.F. Sashenkova SUMMARY OF 20-YEARS’ SURVEY OF
MINERAL COMPOSITION OF THE KARYMSKOYE CALDERA LAKE AFTER ITS 1996 HAZARDOUS
ERUPTION
A.N. Rogozin, V.L. Leonov NEW DATA ON THE EOPLEISTOCENE CATASTROPHIC CALDERAFORMING ERUPTION IN KAMCHATKA
Dmitry Savelyev, Olga Savelyeva , Maxim Portnyagin FRAGMENTS OF CRETACEOUSSEAMOUNTS IN ACCRETIONARY STRUCTURE OF THE KAMCHATSKY MYS PENINSULA(KAMCHATKA, RUSSIA)
Chiharu Tomijima, Mitsuhiro Nakagawa GEOLOGICAL STUDY ON CALDERA-FORMINGERUPTION OF SHIKOTSU VOLCANO, SOUTH-WESTERN HOKKAIDO : SPECIAL REFERENCE TO
VENT FORMATION PROCESS AND MAGMA SYSTEM
Anna Volynets, Maria Pevzner, Andrey Babansky GEOCHEMISTRY OF NEOGENEQUATERNARY MAGMATISM OF THE SOUTHERN PART OF SREDINNY RANGE, KAMCHATKA
Victor N. Chebrov, Anna A. Skorkina, Danila V. Chebrov, Dmitry V. Droznin, Dmitry A.
Ototuk REAL-TIME EARTHQUAKE MONITORING FOR TSUNAMI WARNING IN KAMCHATKA
DURING 2011-2015
Kei Ioki, Yuichiro Tanioka, Gentaro Kawakami, Yoshihiro Kase, Kenji Nishina, Wataru Hirose,
Satoshi Ishimaru, Hideaki Yanagisawa TSUNAMI SIMULATION AND LANDSLIDE MODEL OF
THE 1741 OSHIMA-OSHIMA ERUPTION
Yoshihiro Kase, Keiichi Hayashi, Gentaro Kawakami, Kenji Nishina, Atsushi Urabe, Yasuhiro
Takashimizu CHARACTERIZATION OF ELECTRIC CONDUCTIVITY, PH, AND ORGANIC-WALLEDMICROFOSSILS FOR IDENTIFYING TSUNAMI DEPOSITS: AN EXAMPLE OF MODERN TSUNAMI
AND PALEOTSUNAMI DEPOSITS IN PACIFIC COAST LOWLANDS, HOKKAIDO AND TOHOKU,JAPANOlga Girina, Evgenii Gordeev, Alexander Manevich, Dmitry Melnikov, and Anton Nuzhdaev
2015-2016 ACTIVITY OF KAMCHATKAN AND NORTHERN KURILES VOLCANOES (RUSSIA)
AND DANGER TO AVIATION
Hiroki Miyamachi, Koshun Yamaoka, Hiroshi Yakiwara, Yuta Maeda, Toshiki Watanabe,
Takahiro Kunitomo, Takeshi Tameguri3, Masato Iguchi TEMPORAL VARIATION OF THE
ACROSS SIGNALS DURING A PERIOD FROM JANUARY TO AUGUST, 2015 IN SAKURAJIMA
VOLCANO, JAPAN.
Hugh Harper and Jeff Freymueller REVISITING COSEISMIC AND POSTSEISMIC
DEFORMATION FROM THE 2002 DENALI, ALASKA EARTHQUAKETHURSDAY, JUNE 2
EXCURSION
Field excursion to Chena Hot Springs
09:00
10:00

09:00 – 22:00

Bus picks up participants at the southern entrance to the Reichardt Building. Rideto the hot springs, on-bus discussions.
Arrival to the hot springs. Visit to hydrothermal power plant and other local
attractions.
9

12:00
13:00
17:30
20:30

Lunch (boxes)
Discussions continue in the hot springs
Dinner at the Chena Hot Springs restaurant
Bus ride back to Fairbanks

FRIDAY, JUNE 3
TECHNICAL SESSIONS
Morning coffee
07:30

REIC lobby, 07:30 – 08:00

Breakfast.

Volcano Monitoring (Oral presentations)

REIC 201, 08:00 – 10:00

Chairs: Peter Webley and Taryn Lopez
08:00 John Lyons, Matthew Haney, David Fee, Cindy Werner, Christoph Kern, Diana
Roman, and John Power RECENT ADVANCES IN GEOPHYSICAL MONITORING AT
MOUNT CLEVELAND VOLCANO, ALASKA
08:20 Alex M. Iezzi, Hans F. Schwaiger, David Fee, Matthew Haney CONSTRAINING THE
SPATIAL AND TEMPORAL VARIABILITY OF ATMOSPHERIC CONDITIONS TO EXPLORE
THE INFRASOUND DETECTION OF VOLCANIC ERUPTIONS IN ALASKA
08:40 Kathleen McKee, David Fee, Akihiko Yokoo, Robin Matoza ANALYSIS OF FUMAROLE
ACOUSTICS AT ASO VOLCANO, JAPAN
09:00 Jonathan Dehn, Peter Webley, and Anna Worden ERUPTION TRENDS IN THE KURILE,
KAMCHATKA, AND ALASKAN ARCS
09:20 Shigeki Tasaka, Masaya Matsubara, Yasuhiro Asai, and Fumiaki Kimata INCREASING
OF GAS BUBBLINGS AT WARIISHI FLOWING SPRING, CENTRAL JAPAN, PRIOR TO THE
2014 ONTAKE VOLCANO ERUPTION
09:40 P. W. Webley, O. Girina, J. S. Shipman REMOTE SENSING ANALYSIS OF THE 20152016 SHEVELUCH VOLCANO ACTIVITY
10:00

Coffee break

Volcano Monitoring (Oral presentations) continued

REIC 201, 10:20 – 12:00

Chairs: Peter Webley and Taryn Lopez
10:20 David Fee, Matt Haney, Robin Matoza, Dave Schneider, Peter Cervelli, Alex Iezzi
INFRASOUND AND SEISMIC OBSERVATIONS OF THE MARCH 2016 ERUPTION OF
PAVLOF VOLCANO, ALASKA
10:40 P. Webley, J. Dehn, M. Harrild, A. Worden, D. McAlpin THERMAL REMOTE SENSING
AND ASH DISPERSION MODELING OF THE 2016 ERUPTION OF PAVLOF VOLCANO
11:00 Taishi Yamada, Hiroshi Aoyama, Takeshi Nishimura, Masato Iguchi, Muhamad
Hendrasto ESTIMATION OF VOLUME FLUX OF VOLCANIC ERUPTIONS WITH VERYLONG-PERIOD ACOUSTIC SIGNALS
10

11:20

11:40

12:00

Ryo Tanaka, Takeshi Hashimoto, Tsuneo Ishido, Nobuo Matsushima NUMERICAL
MODEL OF TEMPORAL CHANGES IN MAGNETIC TOTAL FIELD AND GROUND
DEFORMATION DUE TO HYDROTHERMAL SYSTEM IN VOLCANOES (1). - A CASESTUDY ON TOKACHI-DAKE VOLCANO, JAPANRui Fernandes, Machiel Bos, Rafael Couto, Jeff Freymueller, and Maksim Tretyakov
EVALUATING THE INFLUENCE OF DATA GAPS IN THE ANALYSIS OF POSITION TIMESERIES DERIVED FROM GPS CONTINUOUS STATIONS
Lunch

Tsunami (Oral presentations)
13:00

13:20

REIC 201, 13:00 – 13:40

Dmitry Nicolsky, Elena Suleimani, Jeffrey Freymueller and Richard Koehler
HYPOTHETICAL TECTONIC TSUNAMI SOURCES ALONG THE EASTERN ALEUTIANISLAND ARC AND ALASKA PENINSULA FOR INUNDATION MAPPING AND HAZARDASSESSMENT
Elena Suleimani, Dmitry Nicolsky, Rich Koehler REGIONAL TSUNAMI HAZARD MAP
FOR COMMUNITIES ON ALEUTIAN ISLANDS AND ALASKA PENINSULA

Discussion, concluding remarks and wrap up

REIC 201, 13:40 – 14:40

Presiding: Jeff Freymueller, John Eichelberger, Minoru Kasahara, and Evgenii Gordeev
14:40 Coffee break
Additional time for focused group meetings and discussions

REIC 201, 14:40 – 17:30

Farewell dinner on the Tanana Chief Riverboat

17:30 – 21:00

17:30

21:00

Depart for farewell dinner on the riverboat. Bus picks up participants at thesouthern entrance to the Reichardt Building. Local participants are encouraged touse their own transportation.
Bus ride back to the Reichardt Building.
Adjourn!
Katmai trip starts next morning!

11

ABSTRACTS

Keynote Talk

12

BASED ON GLOBAL OBSERVATIONS, TWO REASONS WHY THE ALEUTIANALASKA SUBDUCTION ZONE IS PRONE TO RUPTURE IN GREAT (> Mw8.0)
MEGATHRUST EARTHQUAKESDavid W. Scholl1,2, STEPHEN H. KIRBY1 ROLAND VON HUENE1
1
U.S. Geological Survey, Emeritus, Menlo Park, California 94025, USA
2
Department of Geology and Geophysics, Emeritus, University of Alaska Fairbanks,
Fairbanks, Alaska 99775, USA
INTRODUCTION
Wonderments have long been expressed about the influence, if any, geologic factors
have on the occurrence and non-occurrence areas of high-magnitude great (>Mw8.0), giant(>Mw8.5) and supergiant (>Mw9.0) megathrust earthquakes. A large base of global
observations, one that grew rapidly in the past 12 years, identifies two significant factors that
respectively (1) inhibit and (2) favor high-magnitude rupturing. Both involve smoothness
attributes of the subducting surface of the underthrusting oceanic plate. These are, respectively,(1) Inhibiting Factor, the underthrusting of high, areally large bathymetric relief
hinders rupture continuation and the generation of high-magnitude megathrust earthquakes(see, for example, Wang, K., and Bilek, S.L., 2014, Fault creep caused by subduction of roughseafloor relief: Tectonophysics, v. 610, p. 1–24), and,(2) Favoring Factor, underthrusting thick sediment and/or bathymetric smooth seafloor
promote rupture continuation and the generation of high-magnitude megathrust earthquakes.
Based on a small and inaccurate data base, The smoothness factor was first explored by Ruff
(1989, Do trench sediments affect great earthquake occurrence in subduction zones?: Pure andApplied Geophysics, v. 129, p. 263–282). A relationship was recognized but was not statisticallycompellingly.
CHECKING OUT THE SMOOTHNESS FACTOR
A newly compiled and much larger global base of well-vetted observations now
statistically supports the posit that high-magnitude megathrust earthquakes are favored to occur
where the underthrusting seafloor is:(1) made smooth by a thick blanket of subducting, relief-smothering sediment or(2) by an expanse of seafloor that is bathymetrically smooth (Scholl et al., 2015. Great(≥Mw8.0) megathrust earthquakes and the subduction of excess sediment and bathymetricallysmooth seafloor, Geosphere: v. 11, no. 2, p. 236–265).
Smoothing is effected, perhaps dominantly, by the subduction of a trench-axis sedimentsection thicker than ~1km. Where the thickness is much thinner, smoothing can be producedby the underthrusting of low basement relief and where augmented by a subduction channel
thickened by forearc subduction erosion (Fig. 1).

13

IMPLICATIONS FOR ALEUTIAN-ALASKA SUBDUCTION ZONE
Both factors work together to favor the common rupturing of high-magnitude megathrustearthquake along the Aleutian-Alaska subduction zone. Inhibiting factor 1, subducting rupturehindering relief, is principally located at widely spaced fracture zones and the seamountprovinces of the Gulf of Alaska (Fig. 2). Favoring factor 2, subduction of thick sediment, isprovided by glaciated Alaskan drainages that charged the trench axis with a ~2 km thicksediment body from the eastern end of the Alaska trench westward along much of the length of
the Aleutian Trench. Active subduction erosion also further thickens and smooths the
subduction channel separating the Pacific and North American plates.
It is worth noting that characteristically intra-oceanic subduction zones, e.g., the Izu-BoninMariana (IBM) and Tonga-Kermadec arc-trench systems, are not prone to rupture in great
megathrust earthquakes. The trenches of these subduction zones are only thinly sedimented andthey are entered by large, rupture-inhibiting bathymetric elements, in particular the IBM
system. The circumstance that the Aleutian-Alaska trench axis is charged with sediment
between widely space bathymetric elements are prominent contributors to the repeatednucleation of great megathrust earthquakes that commonly generate destructive near and farfield tsunamis.

14Figure 2. High-magnitude megathrust earthquakes repeatedly
nucleate along the Aleutian-Alaska subduction zone, which is
thickly charged with subducting sediment between widely spaced,large bathymetric elements entering the subduction zone.

15

SEISMOLOGY(Oral presentations)16

PEAK RATES AND LARGEST MAGNITUDE EVENTS IN EARTHQUAKESWARMS FROM DIFFERENT TECTONIC SETTINGS
Stephen R. McNutt1, Glenn Thompson1, Jochen Braunmiller1, Stephen Holtkamp2
1
School of Geosciences, University of South Florida, Tampa, FL, USA
2
Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK, USA.
We present results of recent studies of earthquake swarms from local data at volcanoes, andteleseismic data from MOR and volcanic regions, with the focus on identifying diagnostics.
One clear pattern for local volcanic swarms is that peak rates often occur early, whereas thelargest M event occurs late. Using a dataset of 20 swarms from the literature, swarm durations
ranged from 12 h to 180 d, measured from swarm onset to eruption onset. Data were normalized
to % duration. Peak rates occurred from 1-42 % of the way through swarms (with 2 outliers),
whereas the largest M event occurred from 32-99 % of the way through. Additional evidence
from 4 cases suggests that the seismic source size grows systematically, especially for eventswith similar waveforms (families). This is revealed in plots of M or amplitude versus time for
event families. For comparison, 19 cases of mid-ocean ridge swarms and 67 cases of teleseismic
volcanic swarms were analyzed. The MOR data show durations of 1-42 d, with peak rates
occurring 1-24 % of the way through and largest M occurring 1-87 % of the way through. In 6
cases largest M occurs before or at the same time as peak rate. The teleseismic volcanic data
show durations of <1 to 577 d, with peak rates occurring 1 to 100 % of the way through andlargest M occurring 1-100 % of the way through. Thus the patterns for MOR and teleseismic
volcanic swarms are similar to each other but differ significantly from that for local volcanic
swarms. Further work on volcanic swarms shows that the distribution of seismicity before thepeak rate differs from after, suggesting two dominant processes. The durations of post-peak
portions are roughly proportional to the peak rates. This is similar to the behavior of aftershock
sequences and suggests that diffusion is a controlling process. The portions of the swarms prior
to the peaks behave differently, however. These may represent the invasion of hot fluids andthe opening or reopening of cracks prior to magma intrusion. We infer that the growth in event
size reflects activation of a preferred magma pathway. Recognition of such patterns, linked toprocesses, may help to improve monitoring and reduce risks from eruptions. Comparison isrecommended between the patterns observed here and those associated with induced seismicity
from fracking and deep well injection.

17

MAGMA, THERMAL STRUCTURE, STRAIN CONCENTRATION AND ACTIVESEISMICITY IN KUSSHARO CALDERA, HOKKADIO, JAPANHiroaki Takahashi1, Mako Ohzono1, Koji Minato2, Noritoshi Okazaki3, Takahiro
Suzuki3, Tetsuya Takahashi3, Fujio Akita3
1
Institute of Seismology and Volcanology, Hokkaido University, Sapporo, Japan.
2
Muroran Local Meteorological Office, Japan Meteorological Agency, Japan.
3
Geological Survey of Hokkaido, Sapporo, Japan.
The Kussharo caldera in eastern Hokkaido is one of the largest active caldera of Japan
with 26 by 20km diameters. Caldera formation had been occurred since 0.34 to 0.03Ma. Postcaldera volcanism of active doming and smaller caldera formation has been continued.
Magneto-telluric surveys revealed magma body of about 10km diameter in uppermost crust of
deeper than 7km (Honda et al., 2011). InSAR analysis detected unrest volcanic uplift of 25cm
and successive subsidence with seismic activation during 1993-1998 (Geographical Survey
Institute of Japan. 2006). Inflation and deflation of assumed magma body well explained thiscrisis. These facts suggested the magma have potential for future major activity.
Active seismicity inner caldera has been also recorded. Four tectonic M>6 eventsoccurred concentrating in southwestern rim of caldera. Seismicity level of this caldera is highest
in Hokkaido. Nationwide strain rate map estimated by the Japanese nationwide continuous
GNSS network operated by Geospatial Information Authority of Japan (GEONET) clearly
indicated this caldera is one of the highest strain rate zone over Japanese Islands with 3-07/yr.
High density GNSS observation network deployed in caldera also suggested high strain rateand spatial complex strain field. Observed strain field might be due to multiple interaction of
tectonic strain generated by plate coupling along Kuril trench and volcanic activity.
Separation of tectonic and volcanic factors is required to evaluate crustal activity.
Inhomogeneous crustal structure might be one of control factor for heterogeneous strain field
due to tectonic process. Caldera basin structure of 4km deep filled by soft volcanic sediments
was confirmed by dense gravity surveys (Honda et al., 2011). Magma body in upper crust isalso important inhomogeneous element. Effects of these physical foreign materials in crust forstrain field were evaluated by FEM modeling. Boundary condition of regional strain field
driven by plate coupling along Kuril trench was assumed. Simulation suggested a magma bodyin uppermost crustal medium generated little influence to strain field on earth’s surface. Caldera
basin, however, could cause strain concentration. These results suggested strain concentration
observed on caldera surface might be primary due to caldera basin structure. Analysis with bothcaldera structure and a magma body implied stress concentration between caldera basin and amagma body.
Thermal structure could control deformation style of rock, brittle-ductile transition
depth in upper crust and strength of rock failure. Subsurface temperature structure in thiscaldera had been evaluated using well-based thermal gradient data. Maximum 8degree/100m
thermal gradient was observed in caldera center and 4degree/100m outside. Depth profile ofbrittle and creep strength under hydrostatic regime implied very thin elastic layer of less than
4km thick. Epicenters of past medium earthquakes were concentrated at the edge of caldera,
and might suggest possible thermal structure controlling. Stress rate value estimated from FEM
simulation was about 0.02MPa/yr, and significantly smaller than strength of rock failure.
Mechanism for strength weakening, e.g. existence of high pressure liquid in uppermost crust,is required to explain active tectonic seismicity in this caldera.

18

THE REVEALING OF THE VOLCANIC ACTIVITY FOR KLYUCHEVSKAYAGROUP OF VOLCANOES FROM CONTINUOUS SEISMIC RECORDS
Nikolai Shapiro1,2, Dmitry Droznin3, Svetlana Droznina3, Victor Chebrov3, Evgeny
Gordeev2, William Frank1
1
Institute de Physique du Globe de Paris, Paris, France
2
Institute of Volcanology and Seismology, Petropavlovsk- Kamchatsky, Russia
3
Geophysical Survey, Petropavlovsk-Kamchatsky, Russia

We analyze continuous seismic records from 18 permanent stations operated in vicinity of the
Klyuchevskoy group of volcanoes (Kamchatka, Russia) during the period between 2009 and2014. We explore the stability of the inter-station cross-correlation to detect different periodsof sustained emission from seismic energy. The main idea of this approach is that crosscorrelation waveforms computed from a wavefield emitted by a seismic source from a fixed
position remain stable during the period when this source is acting. The detected periods ofseismic emission correspond to different episodes of activity of volcanoes: Klyuchevskoy,
Tolbachik, Shiveluch, and Kizimen. For Klyuchevskoy and Tolbachik whose recent eruptions
are mostly effusive, the detected seismic signals correspond to typical volcanic tremor, likely
caused by degassing processes. For Shiveluch and Kizimen producing more silicic lavas, theobserved seismic emission often consists of many repetitive long period (LP) seismic events
that might be related to the extrusion of viscous magmas. We develop an approach for automatic
detection of these individual LP events in order to characterize variations of their size andrecurrence in time.

19

SEISMIC ATTENUATION, TIME DELAYS AND RAYPATH BENDING OFTELESEISMS BENEATH CERRO UTURUNCU, BOLIVIA
Alexandra K. Farrell1 and Stephen R. McNutt1
1
School of Geosciences, University of South Florida. Tampa, FL, USA
Cerro Uturuncu (22° 16’ 12” S, 67° 10’ 48” W), Bolivia, is a Pleistocene-aged volcano
which has attracted considerable scientific attention over the last few years. It was one of only
four volcanic centers to show deformation based on an InSAR survey of over 900 SouthAmerican volcanoes by Pritchard and Simons (2000). Mogi source modeling showed that the
volcano was inflating 1.5-2 cm/yr centered ~3 km to the southwest of the volcano’s summit
and at mid-crustal depths of 17-20 km. A reconnaissance survey in 2004 showed a high rate ofseismicity despite the volcano’s quiescence during the past 270 K years (Sparks et al., 2008).
Uturuncu also overlies the largest known crustal magma body in the world, the Altiplano-Puna
Magma Body, which among other characteristics is a zone of low seismic velocities (Zandt etal., 2003). Determining the interaction between seismic waves and the seismic low-velocity
zone (and possible magma body) beneath Cerro Uturuncu is important because suchinteractions affect the results of seismic imaging methods and can be used as additional sourcesof information to constrain the location and properties of partial melt.
A set of 14 teleseismic earthquakes sourced to the NE (1, Calabria Subduction Zone),
NW (4, Japan Subduction Zone), SE (5, South Sandwich Subduction Zone), and SW (4,Kermadec-Tonga Subduction Zones) was studied to determine how wave propagation wasaffected by a presumed magma body beneath Uturuncu. The number of events is small but theevents have good signal-to-noise ratios and very similar waveforms for each event so that
reliable measurements could be made of arrival times and amplitudes. Attenuation of
amplitudes occurs in a NW-SE trend beneath the volcano, 14 by 33 km, with calculated valuesof quality factor Q as low as 1.7, suggesting strong seismic attenuation. Relative time delays(between the theoretical and observed travel times) of up to 0.8 sec were also observed. The
pattern of attenuation and relative time delays together showed four trends: fast and notattenuated (normal crust), slow and attenuated (partial melt), fast and attenuated (likely highfracture density), and slow but not attenuated (possible deep low Vp structure). Results suggest
partial melt as high as 16-60% in a region of low Bouguer gravity, high Vp/Vs, persistentseismicity, and overlapping a locus of uplift. Realistically, percent partial melt values above
30% are unlikely and therefore, to account for this, the anomaly would need to have a greater
thickness along the raypath for the stations showing 30% or more, thus giving a mean partial
melt zone thickness of 24.7 km for an assumed uniform percent partial melt value of 20%.

20

WIDESPREAD IMAGING OF THE LOWER CRUST, MOHO, AND UPPER
MANTLE BENEATH ALASKA FROM RAYLEIGH WAVES
Matthew M. Haney1, Victor C. Tsai2, Kevin M. Ward3
1
Alaska Volcano Observatory, U.S. Geological Survey, Anchorage, AK, USA
2
California Institute of Technology, Seismological Laboratory, Pasadena, CA, USA
3
University of Arizona, Department of Geoscience, Tucson, AZ, USA
The inversion of surface-wave dispersion curves for a shear-wave velocity depth profile
is a classic geophysical inverse problem. Recently, Haney and Tsai (2015; Geophysics)
developed a new approach to this problem based on assumptions that are similar to those usedin the formulation of the Dix equation in reflection seismology. In contrast to conventionalsurface-wave inversion, the Dix-type relation for surface waves does not require an initialmodel and solves directly for shear-wave velocity, not a perturbation in shear-wave velocity.
Haney and Tsai (2015) demonstrated the method for both under- and over-parameterized cases
and used under-parameterization to solve for Moho depth and crustal and mantle shear-wave
velocity across the Western US from only three phase velocity maps.
Here we extend the under-parameterized method presented in Haney and Tsai (2015) tothe over-determined case when more than three phase velocity maps are available. We apply
the Dix technique to phase-velocity maps of the contiguous US and Alaska at periods between
12 and 45 s. We use the Dix inversion result as an initial model for subsequent nonlinear
inversion. In the contiguous US, we image an apparent deepening of the Moho to the west of
Cascade volcanic chain that we interpret as the waveguide interface transitioning to the slab
due to the continental Moho becoming transparent above the mantle forearc. Our result in
Alaska is the first regional Moho map explicitly derived from seismic waves. We find thatcrustal thickness is generally correlated with topography, with thicker crust beneath mountain
ranges (Alaska Range, Talkeetna, Kenai, and Wrangell Mountains). North of the Denali Fault,
the Moho is smoother than to the south and located at typical depths of 30-35 km. There arealso indications that the waveguide interface we solve for beneath Prince William Sound isactually the subducting slab, as was also the case in the Cascades. The slab structure beneathPrince William Sound extends further east than the Pacific slab represented in the Slab1.0
model.

21

USING EARTHQUAKES TO PROBE SUBDUCTION MEGATHRUST BEHAVIOR:A LOOK AT EARTHQUAKE SWARMS AND REPEATING EARTHQUAKES IN
ALASKA
Stephen Holtkamp1
1
Geophysical Institute, Univ. of Alaska. Fairbanks, AK, USA.
Recent studies have proposed that analysis of smaller seismic events along a plateboundary can provide valuable insight regarding the state of stress, history of stressaccumulation and release, and the segmentation potential of large faults. For example,
analysis of background seismicity has allowed researchers to produce maps of stressaccumulation and release at a very fine scale. Furthermore, the observation that earthquake
swarms may be related to large earthquake rupture asperities and persistent segmentation
boundaries worldwide suggests that cataloging these events may help characterize the rupture
extent of future great earthquakes. Repeating earthquakes, which represent repeated rupture of
the same asperity, are thought to occur within creeping sections of the fault. Repeating
earthquakes can be used to map the creep history of faults before and after large earthquakes.
Here, I examine repeating earthquakes and megathrust earthquake swarms along the
Alaskan/Aleutian subduction megathrust, where at least several dozen earthquake swarms
have occurred over the past 50 years. Megathrust earthquake swarms in Alaska have occurred
immediately prior larger megathrust earthquakes, such as the 2003 Mw 7.8 and 2006 Mw 6.6
Rat Islands earthquakes. Megathrust earthquake swarms also appear to delimit large
earthquake rupture across a variety of spatial scales. Two sequences of earthquake swarms
were associated with large geodetic signatures, which we interpret to be slow slip. In addition,
we are able to find several families of repeating earthquakes in the Aleutians, despite theobservational challenges. We hope that further analysis of repeating earthquake families andearthquake swarms will aid in understanding the state of stress and creep along themegathrust, and result in a better understanding of the relation between large earthquake
rupture and earthquake swarms.

22

CORNER FREQUENCIES OF SOURCE SPECTRA OF MODERATESUBDUCTION-ZONE EARTHQUAKES OBSERVED NEAR THE AVACHA BAY,
KAMCHATKA
Anna Skorkina1, Alexander Gusev2,11
Kamchatka Branch, Geophysical Survey, Russ.Ac.Sci., Petropavlovsk-Kamchatsky, Russia.
2
Institute of Volcanology & Seismology, Russ.Ac.Sci., Petropavlovsk-Kamchatsky, Russia.
Determination of parameters of earthquake source spectra are crucial for bothunderstanding of earthquake source physics and solving problems of engineering seismology,
strong ground motion prediction in particular.
The Fourier acceleration spectrum of a local earthquake, after correction for distancerelated loss, is typically approximated with 2 low-frequency slope, a corner at frequency fc(that often is split into double corner at fc1 and fc2), and plateau (Aki, 1967; Brune, 1970). Later
Hanks (1982) emphasized the “fmax” phenomenon: this plateau shows high-frequency cutoff at
a certain frequency fmax. Gusev (1983) and Papageorgiou and Aki (1983) ascribed its origin to
the source; later Aki (1988) noticed that fmax slowly decreases with magnitude, and treated thisfact as supporting this idea. At the same period Anderson and Hough (1984) have shown that anear-site constant-Q attenuation layer of limited thickness commonly exists, that introduces
distance-independent loss that can explain the fmax feature without any source-related effects.
However, evidence is accumulating that indicates that the “fmax” feature is a complex
one, caused by both “source-controlled fmax” and “site-controlled fmax”. Along this line Gusev
and Guseva (2014) showed existence of “source-controlled fmax”, relabeled as fc3, for many
Kamchatka subduction earthquakes using records of low-gain channel of IRIS BB station for
1993-2005.
In the present study, following (Gusev and Guseva, 2014), source spectra wereapproximated by a three-cornered shape. Data used are from 372 subduction earthquakes of
2011-2014, recorded by 6 rock-ground Kamchatka stations, including PET, equipped withaccelerometers CMG5T or CMG5TD. The range of magnitudes Mw(L) is 3.7–6.5 (calculatedusing equation Mw(L) = ML - 0.32 which works well for this region), the range of hypocentral
distances is 50–250 km.
To enable reduction of a recorded spectrum to the source, loss parameters were
estimated beforehand. Parameters of the attenuation model used are Q0 = 156, γ = 0.56,
q = 0.08 and k0 = 0.03 s. The attenuation model used combined0 = 0.03 s andQ(r=100km) = 156 f 0.56, and included a gradual diminution of loss with distance (Gusev andGuseva, 2015). Spectral amplifications of individual stations due to site effects were estimated;
and recorded spectra were reduced to conditions of the hard-rock PET station. Overall, 1252 S
source spectra were analyzed; and corner frequency sets were obtained for each, consisting of{fc1, fc2, fc3} triples. Not all of them are the complete ones: there were cases when no reliable fc1
estimate was possible; and cases when no high-frequency cutoff (i.e. fc3) was discernible. In
total, 839, 1252 and 1028 estimates have been collected for fc1, fc2 and fc3, respectively.
Coefficients of variation (relative rms scatter) among several single-station estimates offc1, fc2 and fc3 are 0.17, 0.14 and 0.11, considered as acceptable. However, the question stillarises if the estimates obtained reflect the source properties, not random fluctuations (noise),
especially for fc3, reality of which is not generally recognized.
For this purpose pair correlation analysis was used. From the data set we formed pairsof PET estimates and estimates of any other station, for the same event. The main interest was
to check whether a fc3 estimate obtained at a station for a particular event matches tocorresponding fc3 estimate at PET. The coefficient of correlation between such pairs of fc3
estimates (fig. 1c) occurred to be 0.62, with the lower bound of the 95% confidence interval
23equal to 0.58, proving the match of estimates between stations, and demonstrating therefore
that fc3 values are of source origin. Similar correlation coefficient for fc2 is 0.67 (fig. 1b), withthe lower bound of the 95% confidence interval equal to 0.63.
The mass estimates of the first, fc1, second, fc2 and third, fc3, corner frequencies werealso used to study their scaling properties, and in particular, scaling exponents= 1/3) is formally brokenk = dlgfck/dlgM0 (where k = 1, 2, 3). The assumption of similarity (for fc1 ( 1 = 0.26); but this result is unreliable because of significant incompleteness of low-fc1
values. Such data loss is related to the fact that on many spectra at their low-frequency edge, Swave spectral level was evidently distorted by probable contribution of surface waves. Other
data suggest that similarity is hardly significantly violated for fc1. However, deviations fromsimilarity are pronounced for fc2 ( 2 = 0.22±0.01), and even more so for fc3 ( 3 = 0.13±0.01).
This information put significant constrains on possible rupture models for these earthquakes.
The study was supported by the grant from the Russian Science Foundation (project 1417-00621), and was carried out at the Kamchatka Branch of the Geophysical Survey of Russian
Ac. Sci.

Fig. 1. Correlation between individual estimates of fc1 (a), fc2 (b), fc3 (c), obtained at the PET
station (abscissa) and similar estimates obtained at each of other stations such as DAL, KDT,
KRM, RUS and SPN (ordinate)
References
Aki, K. 1967. J. Geophys. Res., v. 72. P. 1217-1231.
Aki, K. 1988. Physical theory of earthquakes // Seismic Hazard in Mediterranean Region,
Kluwer Academic Publishers. P. 3-33.
Anderson, J. and Hough, S. 1984. Bull. Seismol. Soc. Amer., v. 74. P. 1969-1993.
Brune, J. 1970. J. Geophys. Res., v. 75. P. 4997-5009.
Gusev, A.A. 1983. Geophys. J. Royal Astr. Soc., v. 74. P. 787-808.
Gusev, A.A. and Guseva, E.M. 2014. Doklady Earth Sciences, 458. P. 1112-1115.
Gusev, A.A. and Guseva, E.M. 2015. Splitting fmax: separating site-controlled and sourcecontrolled contribution into the upper cutoff of acceleration spectrum of a local earthquake// 26th IUGG General Assembly, Prague.
Hanks, T. 1982. fmax // Bull. Seismol. Soc. Amer., v. 72. P. 1867-1879.
Papageorgiou, A. and Aki, K. 1983. Bull. Seismol. Soc. Amer., v. 73. P. 693-722.

24

ESTIMATION OF THE LONG-TERM EFFECT OF VISCOELASTIC RELAXATIONINDUCED BY THE 2011 TOHOKU EARTHQUAKE AND OTHER INTERPLATE
EARTHQUAKES AROUND NORTHEASTERN ASIA
Mako Ohzono1, Hiroaki Takahashi1, Nikolay V. Shestakov2,3 Guojie Meng4, Mikhail. D.
Gerasimenko3
1
Institute of Seismology and Volcanology, Hokkaido University, Sapporo, Japan.
2
Far Eastern Federal University, Vladivostok, Russia.
3
Institute of Applied Mathematics, Far Eastern Branch, Russian Academy of Sciences,
Vladivostok, Russia.
4
Institute of Earthquake Science, China Earthquake Administration, Beijing, China.
After the large earthquakes, postseismic deformation is induced by their stressdisturbance. The large coseismic and postseismic deformation caused by the 2011 Tohoku-oki
earthquake (magnitude 9.0) observed by GNSS not only in Japan, but also in the northeast Asia.
Even though five years passed, the horizontal velocity at an IGS site, Changchun (CHAN),
which is located ~1600 km away from the focal area, indicates faster velocity than that ofinterseismic period (~3mm/year). It means that the postseismic deformation has now beenongoing in the broad area.
Although there are several mechanisms of the postseismic deformation, the viscoelastic
relaxation largely affects for long-term and widespread area around the focal area. Therefore,
stable tectonic movement, such as plate motion, must be contaminated by this phenomenon.
Quantitative estimation of this effect with preferable subsurface viscoelastic structure isimportant to understand the tectonic behavior with the earthquake cycle around the focal area.
In this study, we assume the long-term widespread postseismic deformation is mainly
caused by the viscoelastic relaxation. Then, we predict the spatio-temporal evolution of theviscoelastic relaxation by the 2011 Tohoku-oki earthquake using VISCO-1d (Pollitz, 1997).
Coseismic fault parameters are taken from several previous studies. The signal of surface
displacement depends on subsurface structure, such as thickness of elastic layer and viscosityof the asthenosphere. We test several sets of those parameters. As an example, when we set 50
km thickness of elastic layer and 1018 Pa s of viscosity in the underlying viscoelastic layer, wefind large and long-term deformation (~30 cm in horizontal, and ~5 cm in subsidence for 100
years).
Japan is a typical plate subduction zone, therefore many large interplate earthquakes
have already occurred including the 2011 Tohoku-oki earthquake. In the historical record, there
are 15 earthquakes over magnitude 8.0 have occurred since 869 in and around Japan. In orderto check the effect of their possible postseismic deformation, we also estimate the long-term
spatio-temporal surface displacement induced by the viscoelastic relaxation for thoseearthquakes. Preliminary result shows that five earthquakes may contaminate the displacement
field around Vladivostok, Russia, when we set the 1018 Pa s of viscoelastic layer beneath 50 km
thickness of elastic layer. The displacement signal from each postseismic deformation depends
on the magnitude of earthquake, focal distance, fault mechanism, duration, and so on. From thisestimation, it is considered that we are unable to ignore the effect of these postseismic
deformation in extensive region of northeast Asia.

25

LONG PERIOD SEISMICITY AND VERY LONG PERIOD INFRASOUND DRIVEN
BY SHALLOW MAGMATIC DEGASSING AT MOUNT PAGAN, MARIANAISLANDSJohn J. Lyons1, Matthew M. Haney1, Cynthia Werner2, Peter Kelly2, Matthew Patrick3,
Christoph Kern2, and Frank Trusdell3
1
Alaska Volcano Observatory, U.S. Geological Survey, Anchorage, Alaska, USA,2
Cascades VolcanoObservatory, U.S. Geological Survey, Vancouver,Washington, USA,
3
Hawaiian Volcano Observatory, U.S. Geological Survey, Volcano, Hawaii, USA
Long period (0.5-5 Hz) seismicity is frequently observed at active volcanoes and has been
attributed to both resonance in fluid-filled cavities and slow brittle failure. Identifying thelocation and source mechanism of long period (LP) seismicity is important for understanding
and monitoring volcanic activity, but can be challenging because waveforms are often
emergent, have low amplitudes, and may be affected by severe topography or an unknown
shallow velocity structure. In this talk, I’ll present results from a study of LP seismicity thathighlights its utility in interpreting volcanic behavior and illuminating the geometry of shallow
volcanic conduits, particularly when combined with other geophysical and geological data.
Mount Pagan produced LP seismicity and very long period (<0.5 Hz) infrasound (iVLP) duringcontinuous degassing from July 2013 to January 2014. The frequency content of the LP and
iVLP events and delay times between the two arrivals were remarkably stable and indicate
nearly co-located sources. Full waveform inversion of a master LP event reveals a volumetricsource 60 m below and 180 m west of the summit vent. The moment tensor reveals a volumetricsource modeled as resonance of a subhorizontal sill intersecting a dike. We model theseismoacoustic wavefields with a coupled earth-air 3-D finite difference code. The ratios ofpressure to velocity measured at the infrasound arrays are an order of magnitude larger than thesynthetic ratios, so the iVLP is not the result of LP energy transmitting into the atmosphere atits epicenter. Based on crater shape and dimensions determined by structure from motion, we
model the iVLP as acoustic resonance of an exponential horn. The source of the continuous
plume from Multi-GAS and FLYSPEC data analysis is shallow magmatic degassing, which
repeatedly pressurized the dike-sill portion of the conduit over the 7 months of observation.
Periodic gas release caused the geologically controlled sill to partially collapse and resonate,while venting of gas at the surface triggered resonance in the crater. LP degassing only accounts
for ~12% of total degassing, indicating that most degassing is relatively aseismic and thatmultiple active pathways exist beneath the vent.
Figure 1. Model of shallow magmatic degassing and LP generation at Mount Pagan. a) Mapped
geology, elevation profile, and crack system modeled from LP seismicity in an east-west crosssection through the summit crater. b,c) Schematic of degassing processes and sources of LP
seismicity and iVLP (from Lyons, J. J., M. M. Haney, C.Werner, P. Kelly, M. Patrick, C. Kern,and F. Trusdell (2016), Long period seismicity and very long period infrasound driven by
shallow magmatic degassing at Mount Pagan, Mariana Islands, J. Geophys. Res. Solid Earth,
121, doi:10.1002/2015JB012490.)

26

27

SEISMIC EQUIVALENTS OF INFRASONIC SCALING LAWS FOR VOLCANICJETS AND ACOUSTIC MULTIPOLES
Matthew M. Haney1, Robin Matoza2, David Fee3, David F. Aldridge4
1
Alaska Volcano Observatory, U.S. Geological Survey, Anchorage, AK, USA
2
University of California Santa Barbara, Department of Earth Science, Santa Barbara, CA,USA
3
University of Alaska Fairbanks, Geophysical Institute/AVO, Fairbanks, AK, USA
4
Sandia National Laboratories, Geophysics Department, Albuquerque, NM, USA
Seismic and acoustic waves are manifestations of mechanical energy in the solid Earthand atmosphere, respectively. Here, we explore analogies between equivalent source theory inseismology (moment-tensor and single-force sources) and equivalent source theory inacoustics, i.e., monopoles, dipoles, and quadrupoles [e.g., Woulff and McGetchin, 1976].
Although infrasound from volcanic eruptions may be more complex than a simple monopole,
dipole, or quadrupole assumption, these elementary sources are a logical place to begin to relate
seismic and acoustic sources. Treating sources in such a unified way will be necessary in theapplication of seismo-acoustic waveform inversion at volcanoes, in which seismic andinfrasound data are simultaneously reconciled for a common near-surface source (i.e., volcanic
explosion).
By considering the radiated power of a harmonic force source at the surface of an elastic
halfspace, we show that a volcanic plume modeled as a seismic force has the same scaling as
an acoustic dipole. This is surprising since, in seismology, the equivalent force system is a
widely-used representation of moment tensors in terms of force couples and dipoles. Here, weshow from first principles that the seismic force source is in fact dipolar in nature, since it canbe equivalently represented as an explosion dipole and a pair of torque dipoles in a particularconfiguration. This forges a deep connection between the multipole expansion in acoustics andthe use of forces and moments in seismology and suggests that an alternative description ofseismic sources is possible.

28

QUANTIFYING GROUND COUPLED AIR WAVES TO DETERMINE GAS FLUXAT PAVLOF VOLCANO, ALASKA, DURING THE 2007 ERUPTION
Cassandra M. Smith1, Stephen R. McNutt1, Glenn Thompson1
1
School of Geosciences, University of South Florida. Tampa, FL, USA
An abnormally high number of explosion quakes were noted during the monitoring effort
for the 2007 eruption of Pavlof Volcano on the Alaska Peninsula. This eruption lasted from
August 14th to September 13th with the peak in activity between August 28th and September 2nd.
In this study we manually catalogued the explosion quakes from their characteristic groundcoupled air waves. This study investigates how the ground-coupled air waves might be used ina monitoring or analysis effort by calculating energy release and gas mass release. Over 3x104
quakes were recorded. Using Garces et al.'s (2000) equation for vertical ground velocity wecalculated the energy release from the explosions to be 3x1011 J, and the total gas mass(assuming 100% water) released was 450 metric tons. We performed a sensitivity analysis inorder to determine that our variable choices were reasonable and found that when our results
are compared to other volcanoes in the literature they are found to be similar, but occasionallysomewhat lower. Nevertheless, the tracking of explosion quakes has the potential to estimate
relative eruption intensity as a function of time, and is thus a useful component of a seismic
monitoring effort.

29

PERSPECTIVES ON THE MW7.1 INISKIN EARTHQUAKE
Michael West1, Matt Gardine1, Natalia Ruppert1, Carl Tape1, Jeffrey Freymueller1,
Stephen Holtkamp1
1

Alaska Earthquake Center, Geophys. Institute, Univ. Alaska Fairbanks, Fairbanks, AK, USA.

The Mw 7.1 earthquake on January 24, 2016 was the largest intermediate-depth earthquake everrecorded in mainland Alaska and produced the most significant shaking in the Cook Inlet regionin half a century. The earthquake occurred in the subducting Pacific Plate at a depth of 125km.
The earthquake ruptured a natural gas line resulting in an explosion and fire than consumed
four homes. Additional structural damages were primarily the result of slumping soilsIt
occurred at the edge of a long-recognized cluster of intermediate-depth earthquakes, with asimilar down-dip minimum stress direction observed in prior earthquakes. It was larger
however than any previously identified earthquake in this region. From 2001 to 2014 there were
no intermediate-depth M6+ earthquakes in Alaska east of the Fox Islands. Since July 2014,
there have been four including this one. The Iniskin earthquake aftershock zone extends ~60km
northeast and abuts the hypocenter of M6.4 earthquake six months prior. Static displacements
are largest 100 km east on the Kenai Peninsula. Ground motion were highly variable andconsistent with the directionality of the source. Strong motion records corroborate felt reportsof moderate shaking above the hypocenter and significant influences from regional structures
including the Cook Inlet sedimentary basin. Significant population centers, and the limited
damage, were all at least 100 km or more from the epicenter. This presents two significant
public policy challenges. The first is the misperception that individuals experienced, andinfrastructure survived, the near-field forces of a M7+ earthquake. Instrumental records and felt
reports demonstrate clearly that this is not the case. Second, a M7.1 earthquake at intermediate
depth, combined with comparable M6+ earthquakes in the past few years necessitate a reevaluation of the maximum magnitude and frequency of intermediate depth earthquakes
through the south-central region of Alaska.

30

TECTONICS AND EXPERIMENTS(Oral presentations)31PLATE BOUNDARIES IN THE NORTH PACIFIC
Jeffrey T. Freymueller
Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK 99775
The North American and Eurasian plates diverge at spreading centers in the North Atlantic andArctic Oceans, and converge in northeastern Asia. Because the pole of relative plate motion is
located in the same area, relative plate motions are slow and deformation is diffuse. Overall,
the region consists of a collage of small microplates or blocks moving relative to each other,with some of the microplate boundaries being uncertain or controversial, and some proposed
microplates perhaps being regions of diffuse deformation rather than rigid plates. On the Alaskaside of the North Pacific, additional complexity is driven by the collision of the Yakutat terraneat the eastern end of the Alaska-Aleutian subduction zone, and by the effects of obliquesubduction. The Aleutian arc features an extreme variation in the obliquity of plateconvergence, and the western part of the arc has long been recognized as an example of slip
partitioning of highly oblique subduction. The direction of Pacific-North America relative
motion is essentially trench-normal along the Alaska Peninsula in the eastern part of the arc,and reaches almost trench-parallel at the western end of the arc. Along much of the arc, atectonic sliver of the overriding plate moves in a mostly trench-parallel direction with the rateof motion increasing to the west, and additional blocks or microplates (southern Alaska, Bering
plate) accommodate eastward extrusion of material away from the Yakutat block collision. Here
we examine the long-term velocities of sites in southern Alaska, the Aleutian arc and the Bering
Sea region after removing the effects of recent earthquakes and postseismic deformation. We
will re-examine the extent of the proposed Bering plate and evidence for block motions along
the Aleutian arc in the light of an expanded and more precise data set, and recent seismicity andearthquake focal mechanisms. Our block models suggest a more complex pattern of
deformation than previously proposed.

32

STRAINMETER ARRAY OBSERVATION OF THE DIKE INTRUSION AT
SAKURAJIMA VOLCANO ON 15 AUGUST 2015
Higashi Uchida
Kagoshima Meteorological Office, Japan Meteorological Agency, Kagoshima, Japan.
On 15 August 2015, a rapid increase in the number of volcano-tectonic earthquakes andremarkable crustal deformation were observed at Sakurajima volcano in Japan. Strainmeter datafrom Arimura Station (Fig. 1), located 2km SSE of the volcano’s Showa crater, showed crustal
extension with more than 10 micro-strain (Fig. 2). The strain change was 1,000 times greaterthan those associated with typical explosions at the Showa crater, and was the largest everobserved at the station. The Japan Meteorological Agency (JMA) raised the Volcanic Alert
Level from 3 to 4 at 10:15 on August 15 (Japan Standard Time (JST)) and expanded the hazard
area from 2 to 3 km from the crater. JMA also issued its first residential area warning for
Sakurajima, and around 80 residents living near the hazard area took refuge in evacuation
centers.
No actual eruption occurred, and earthquake activity and crustal deformation subsided
at 03:00 on August 17. Emergency observation by the Japan Aerospace Exploration Agency
using the Daichi-2 satellite's Interferometric Synthetic Aperture Radar (InSAR) revealed
deformation of up to about 16cm closer to the satellite on the eastern flank of Sakurajima. The
Geospatial Information Authority of Japan (GSJ) analyzed these data and Global Navigation
Satellite System data, and proposed a dike model to explain the observed deformation. The
width, length and opening volume of the dike are 0.78km, 1.41km and 2x106m3, respectively.
InSAR data cover a wide area at very high spatial resolution, but are limited in terms of
temporal sampling due to the orbital repeat period of the satellite. To elucidate the dike intrusion
process, the time-continuous strain change observed by an array of three strainmeters (EX-R,
EX-T and EX-D) was analyzed. As shown in Fig. 1, EX-R is aligned in the radial direction to
the crater, and EX-T is aligned in the tangential direction. EX-D is at an angle of 45 degrees tothe other strainmeters, and the array is installed at the end of a 200m horizontal tunnel to achievea high signal-to-noise ratio. Each strainmeter has a baseline length of 28m. Ignoring local
distortions of the strain field, three non-colinear strainmeters can be used to determine theprincipal strain.
The strain records (Fig. 2) are characterized by four points in the time-series
representation: (A) Strain change began at 08:00 on August 15 JST. (B) The rate of strainchange increased at 10:25. (C) The rate of EX-R component change turned from negative(contraction) to positive (extension) at 11:15. (D) Deformation ceased at 03:00 on August 17.
The results show that the EX-D component exhibits the largest change among the three. We
confirmed that the total strain change between A and D was consistent with the change
predicted from the dike model proposed by GSJ.
To clarify the dike intrusion process, strain changes for the periods A-B, B-C and C-D
were calculated as shown in Fig. 3. The contraction axis of the principal strain in the A-B period
has a north-south orientation, and exhibits clockwise rotation during the B-C and C-D periods.
This suggests that dike opening progressed from the SSW end to the NNE end as follows: The
SSW end of the dike opened in the A-B period. The dike opening subsequently progressed to
the NNE direction in the B-C period. Finally, the NNE part of the dike opened in the C-D
period. We also found the migration of earthquake hypocenters, which also supports the NNE
progression of the dike opening.

33

Fig. 1. Map of Sakurajima volcano. Location of Arimura station is denoted by solid circle. The
dike model proposed by GSJ is represented by rectangle. The left shows strainmeter array inthe observation tunnel complex at Arimura Station.

Fig. 2. Strain data recorded at Arimura Station in association with volcanic activity on 15
August 2015.

Fig. 3. Principal strain change observed at Arimura Station during the A-B, B-C and C-D
periods. The black arrows indicate principal strain, and the gray arrows indicate strain
observed at each strainmeter.

34

SEDIMENT WAVES AND CLOUD LAYERING IN EXPLOSIVE VOLCANICERUPTIONS: EVIDENCE FROM ANALOGUE EXPERIMENTS
Johan Gilchrist and Mark Jellinek
Earth, Ocean and Atmospheric Sciences, Univ. of British Columbia, Vancouver, BC, Canada
Introduction
Explosive volcanic eruptions inject (multiphase) mixtures of ash, volcanic gases andentrained air high into the atmosphere. On the basis of previous experiments (Veitch andWoods, 2000; Carazzo and Jellinek, 2012, CJ12 hereafter), eruptions apparently occur in"Buoyant Plume", "Total Collapse" and "Partial Collapse" regimes depending on source andenvironmental conditions (Fig. 1). Some Plinian eruptions, such as Soufriere Hills, Montserrat(February 11, 2010, Fig. 1a) and Mt. St. Helens (May 18, 1980), produce multiply-layered ash
clouds and concurrent pyroclastic density currents (Wadge et. al, 2014, Hoblitt, 1986). Using
analog experiments on multiphase volcanic jets we address three questions:
1. How do the differing dynamics of eruption and sedimentation interact to produce
distinct BP, PC and TC regimes?
2. Over what range of source conditions do multiply-layered clouds occur?
3. How are the underlying processes governing sedimentation and cloud layering
ultimately reflected in the structure and architecture of the resulting deposit?
Methods
Following CJ12, we inject dense, isothermal, sediment-laden water jets at a fixed rate intoa 90 x 90 x 70 cm saltwater tank with a linear density stratification simulating the atmosphericdensity profile in the troposphere. We use 80 µm and 225 µm diameter silica particles tosimulate fine and coarse ash, respectively. Two dimensionless parameters govern the regime of
the jet: the source Richardson number, −𝑅𝑖0, is a measure of jet strength and expresses abalance between the driving inertial and stabilizing buoyancy forces acting at the source, andthe particle volume fraction, 𝜙0 , of the jet. We vary the source conditions to explore a −𝑅𝑖0𝜙0 parameter space appropriate to natural eruptions. We will define a PC jet as one where amodest fraction of the injected mixture collapses to the tank floor and the rest intrudes andspreads as an umbrella cloud (Figs. 1c and 2). TC jets, by contrast, are distinguished by amajority (>90%) of erupted material collapsing to the floor (Fig. 1b). BP jets produce anumbrella cloud with nojet fluid reaching the
Figure 1: -𝑹𝒊𝟎 vs. 𝝓𝟎 regime diagramthat partitions experiments into
Buoyant Plume (BP), Partial Collapse(PC) and Total Collapse (TC) regimes.
Circle and X markers represent datafrom this study while square markers
represent data from Carazzo andJellinek, 2012. (a) Feb. 11, 2010
eruption of Montserrat. (b), (c) and (d)are examples of TC, PC and BP regimes,
respectively. (e) and (f) are deposits
corresponding to (a) and (b),respectively, exhibiting concentricrings marking a terraced structure. (g)Multiply-layered cloud corresponding
to (c). Scale bars are 10 cm long.

tank floor (Fig. 1d).
Results
Figure 2: -Ri0

ϕ035

In Fig. 1 we expand the parameter space initially explored by CJ12 to distinguish conditions
for the BP, PC and TC regimes and for multiply-layered clouds. Qualitatively, we find: Multiply-layered clouds are a characteristic feature of PC jets (Figs. 1a and 1g)
 PC jets closer to the BP regime produce relatively thin multiply-layered clouds, while
jets closer to the TC regime produce relatively thick multiply-layered clouds (cf. Figs.
2a and 2b)
 Axisymmetric, terraced deposits are produced by TC jets and PC jets with 𝜙0 > ~0.02(Figs. 1e and 1f), while BP jets produce deposits decreasing in thickness monotonicallyfrom the vent
 Sediment waves occur in all PC and TC regimes and are discrete, periodic collapse
events in which annular, radially tapered, dense waves fall from the plume top to thetank floor, or some height above it depending on −𝑅𝑖0 and 𝜙0 (e.g. Figs. 1b, 1c and 2).
 In PC and TC jets, sediment waves carry entrained buoyant jet fluid to the tank floor,
deposit their sediment load and release the initially entrained jet fluid to intrude at a
Level of Neutral Buoyancy (LNB)
Quantitatively, our results indicate: Transitions from the BP to TC regimes are marked by increases in the wavelength, sizeand velocity of sediment waves, as well as the production of terraced deposits.
 Transitions from the TC to BP regimes are marked by the sediment wave velocity
approaching the value of the individual particle settling velocity and by the release ofjet fluid from sediment waves above the tank floor
Conclusion
Our results support the following conclusions:
1. Multiply-layered clouds are a distinctive
feature of PC jets
2. The periodic release and rise of entrained
buoyant fluid from sediment waves coming
to rest on the tank floor leads to the
production of multiply-layered clouds.
3. PC and TC regimes with pronounced
sediment waves produce terraced deposits.
2: Comparison of PC jets near each end member regime. (a)BP regimes are more typically characterized Figure
PC jet near TC regime. (b) PC jet near BP regime. Note the tall multiby deposits that vary smoothly in thickness layered cloud, lower LNB, larger wavelength and faster velocity of
sediment waves in (a) as opposed to (b). More solid lines indicate
with radius.
younger intrusions.
4. Transitions between BP, PC and TC regimes
are continuous: These regimes are marked by changes in sediment wave properties thatvary smoothly with −𝑅𝑖0 and 𝜙0 and are not sharply distinguished
Our work suggests a comparison of experimental deposits to natural near-vent deposits may
provide insight into the eruption column dynamics of ancient eruptions.

36

CORRELATION STUDY OF COULOMB STRESS CHANGE IMPARTED BY TWONEW SLOW SLIP EVENTS AND SEISMIC RATE CHANGE IN LOWER COOK
INLET OF THE ALASKA-ALEUTIAN SUBDUCTION ZONE
Shanshan Li1, Jeff Freymueller1, Natalia Ruppert1, Jianjun Wang2
1
University of Alaska Fairbanks, Fairbanks, AK, United States,
2
Wuhan University, Wuhan, Hubei, China

We identified two long-term slow slip events (SSEs) in Lower Cook Inlet, southcentral Alaska(1995.0-2004.8 and 2009.85-2011.81) by inverting the GPS site velocities (Li et al. 2016). The
earlier SSE lasted at least 9 years (observations in that area began in 1995) with Mw~7.8 andaverage slip magnitude as ~82 mm/yr. The latter SSE had almost the same area as the earlier
one, which is within 40-60 km depth range, and a duration of ~2 years with Mw~7.2 andaverage slip magnitude as ~91 mm/yr.
The estimated time-dependent slip behaviors of these two SSEs allow us to track thecorresponding Coulomb stress changes and associate them with seismic activity and nontectonic tremor in Lower Cook Inlet. We will use our slip models to calculate the Coulomb
stress change induced by the time-dependent slip (SSEs) on Alaska-Aleutian subduction zone
plate interface. We are interested to see whether the observations of the seismicity in Lower
Cook Inlet are consistent with stress triggering outside the slowly slipping region. We will test
whether the temporal evolution of earthquakes are explained by increased stressing caused bySSEs, implying that the earthquakes are triggered and probability changes for large earthquakes
in southcentral Alaska. If this hypothesis can be tested, it can lead to a useful method to quantify
the increasing the potential hazard during SSEs since the triggered earthquakes have thepotential to be large and destructive ones.

37

GEOLOGY & PETROLOGY &GEOCHEMISTRY(ORAL PRESENTATIONS)38

ORIGIN OF CALDERAS: COLLAPSES OR EXPLOSIONS?
Izumi Yokoyama
Usu Volcano Observatory, Hokkaido University. Sapporo, Japan
Origins of calderas may be different depending on their subsurface structure that may
be characterized by such features as high-density deposits and low ones that may be observed
as high and low gravity anomalies. First, our discussion is focused on four calderas that wereseen forming during the period from 1815 to 1991, before our eyes, including Novarupta,
Alaska. Coincidently, these four calderas are all low-gravity-anomaly type. Some details of thefour calderas are shown in Table 1.Their formation processes and subsurface structure aresummarized by the existing data analyzed by various authors. And these results are confirmedby results of drillings at some other calderas. Then caldera formation of the both types isdiscussed: The high-gravity-anomaly type calderas usually originate from collapse of erupted
ejecta to the summit magma reservoirs although their creative eruptions have not been
identified, and so some historical eruptions accompanied by collapses on the calderas of thistype are mentioned briefly. Next, low-gravity-anomaly type calderas are discussed fromstandpoints of both the models of collapses and explosions. To confirm the possibility
that volcanic fragments collapse into magma reservoirs, we discuss stress propagation from acrushed reservoir toward the earth surface. It is emphasized that dynamic pressure of explosions
is an important factor in the caldera formations, not only volume of the ejecta. Lastly, formation
mechanisms of large calderas of this type are speculated. Large calderas measuring more than
10 km may be completed by amalgamation of componential calderas in geological times.
Table 1: The four calderas observed during their formation
Earthq.
DiameterMax.
Duration
Previous
beforeCaldera& depthearthq.
climactic
eruption
the(km)
magnitude eruption
event
Tambora 1815 6 0.6~0.7?
3 yrs
3 days7 (?)
Krakatau 1883 5 0.25
1680 AD99 days
23 hrs5
Novarupta
2 ca. 0.25?
7 days
14 hrs
7.0
1912
2.5 0.2
ca.1490
71 days
9 hrs
5.7
Pinatubo 1991
AD

Ejecta volume(km3 DRE) +missing
volume(12~60) + 46
(9~19) + 8
15 + 0.7
4.5 + 2.5

39

BERING - A NEW INTERNATIONAL MARINE RESEARCH PROJECT TO
INVESTIGATE THE MAGMATIC AND TECTONIC EVOLUTION OF THE
BERING SEA AND ITS MARGINS
Maxim Portnyagin1, Kaj Hoernle1, Reinhard Werner1, Boris Baranov2, Gene
Yogodzinski3 and BERING participants
1
GEOMAR Helmholtz Centre for Ocean Research Kiel, Kiel, Germany.
2
P.P. Shirshov Institute of Oceanology RAS, Moscow, Russia.
3
University of South Carolina, Columbia, USA.
The BERING project is a new large project lead by the GEOMAR institution in Kieland focused on marine and on-land investigations in Kamchatka, the Kurile and Aleutian Arcs,
the Bering Sea, and the NW-Pacific. BERING is funded by the German Ministry of Education
and Research with contributions from Russian and U.S. institutions. The overarching goal of
BERING is to elucidate the magmatic and tectonic evolution of the Bering Sea and its margins
over the past ≥50 m.y. In particular, BERING investigates the physical and chemical conditions
that control the development of subduction zones, including subduction initiation, evolution of
mature arc systems, and the impact of subduction volcanism on the environment. To achieve
this goal BERING will address the following major scientific questions in four major directionsof study:(1) Early (pre-Aleutian) subduction history of the Bering Sea: What is the nature of theBeringian and Chukotka Margins and their junction?
(2) Aleutian arc inception and evolution: What is the age and composition of the oldest
rocks in the western Aleutian Arc?
(3) Modern Aleutian arc system: What is the origin and occurrence of recent magmatic
activity in the Western Aleutian Arc?
(4) Arc Input: What is the spatial and temporal compositional variability of the
subducting Pacific lithosphere offshore the Aleutian Arc and Kamchatka?
A central part of the project is the R/V SONNE expedition SO-249, which will be
conducted in June – August 2016 in the framework of the Russian-German Agreement on
Marine and Polar Research and in close cooperation with U.S. American colleagues. The twolegs of cruise SO-249 aim to map and sample magmatic structures in the Aleutians, the Pacificseafloor subducting beneath the Aleutians and northern Kamchatka, and in the western marginof the Bering Sea (Fig. 1). The on shore work program at GEOMAR and cooperating
institutions will include geochronological, petrological and geochemical studies on igneous
samples obtained during the cruise. The results of BERING will be integrated with those ofprevious campaigns (e.g. KOMEX and KALMAR projects), and work carried out within theWorld Oceans and GeoPRISMS initiatives.

40

Fig. 1. The working areas of the R/V SONNE SO-249 BERING expedition Legs 1& 2.

41

A CASE FOR INTEGRATED GEOSCIENCE AND ARCHEOLOGICAL STUDIES IN
THE ALEUTIAN ARC
Kirsten Nicolaysen1, Dixie West2, Virginia Hatfield2, Breanyn MacInnes3, Mitsuru
Okuno4, Arkady Savinetsky5, Olga Krylovich5, Pavel Izbekov6, Lyman Persico1, John
Lyons7, Max Kaufman6,7, Christina Neal8, William E. Scott9, John Power7
1
Whitman College, Walla Walla, WA, USA.
2
Biodiversity Institute, Univ. Kansas, Lawrence, KS, USA.
3
Central Washington University, Ellensburg, WA, USA.
4
Fukuoka University, Fukuoka, Japan.
5
Russian Academy of Sciences, Moscow, Russia.
6
Geophysical Institute, Univ. Alaska, Fairbanks, AK, USA.
7
U.S. Geological Survey, Alaska Volcano Observatory, Anchorage, AK, USA.
8
U.S. Geological Survey, Hawaiian Volcano Observatory, Hawaii National Park, HI, USA.
9
U.S. Geological Survey, Cascades Volcano Observatory, Vancouver, WA, USA.
The daunting array of cost, logistical equipment, difficult transportation, and hazardous
summer weather has limited both exploratory and geographically focused research for the
Aleutian arc, which offers a unique combination of millennia of human history and a broadarray of geological problems including current geologic hazards. Worldwide, stakeholders,scientists, policy makers, and the public are experiencing and studying a rapidly changing
circumpolar North. In the last ~120 years, our global society has experienced (1) declines inkey marine mammals and arctic birds, (2) rising sea level and erosion swallowing coastal
villages, (3) rapid ocean warming and ice melt, and (4) ocean acidification, 5) tsunamis
generated by large subduction zone earthquakes, and 6) impacts of volcanic ash and tephra,
particularly on air transportation. As we study this current climatic furor, react to geologic
disasters locally and regionally, and attempt to predict what is in store for Earth’s future, it isvital to recognize that the Aleutian arc offers an important record of geologic hazards and of
how humans reacted locally to such events. This region experienced slow (climatic) and rapid(geological and human induced) impacts that influenced indigenous peoples and the North
Pacific ecosystem. Supported by the National Science Foundation, the U.S. Geological Survey,
the Alaska Department of Geological and Geophysical Surveys, and the Alaska Volcano
Observatory, our unique partnership of professional and academic scientists and students
includes those who study archeology, paleoecology, paleotsunamis, establishing the recent
earthquake record, the tephra record, magmatic evolution of volcanoes, and the geomorphology
of glacial and mass wasting events was. Shared resources and integration of scientific results
greatly magnify our insights into particular disciplinary questions, our understanding of therelationships between the team’s disciplinary results, and our ability to offer meaningful results
to regional stakeholders, scientists, and policy makers.

42

EVIDENCE FOR MAGMA MIXING AND RAPID MAGMATIC ASCENT INGROUNDMASS GLASS COMPOSITIONS FROM THE 2008 ERUPTION OF
KASATOCHI, CENTRAL ALEUTIAN ISLANDS
Owen K. Neill1, Christopher J. Nye2
1
Peter Hooper GeoAnalytical Lab, School of the Environment, Washington State University,
P.O. Box 642812, Pullman, WA 99164-2812.
2
Alaska Volcano Observatory, State of Alaska, Division of Geological and GeophysicalSurveys, 3354 College Road, Fairbanks, AK 99709 (retired).
Despite its small size (~3 km in subaerial diameter) and lack of historic eruptive history,
the 7-8 August, 2008, eruption of the central Aleutian Kasatochi Island volcano was one of themost violent eruptions in recorded Alaskan history. This eruption lasted 21 hours, and included
one earthquake with a magnitude of 5.9 and ~12 earthquakes with a magnitude of 4 or greater,
releasing more cumulative seismic energy than any eruption ever monitored in the 28-year
history of the Alaska Volcano Observatory (AVO) (Ruppert et al., 2011). The eruption also
produced ~1.7 Tg of SO2, the largest point source emission of sulfur during an eruption sincethe 1991 eruption of Cerro Hudson, Chile (Kristiansen et al., 2011), and a total volume oferuptive material of ~0.2 km3 (Waythomas et al., 2011).
Previous studies of the petrology of the 2008 Kasatochi eruption have found that theeruptive products were dominated by two major lithologies; a white, pumiceous andesite
containing ~58-62 wt% SiO2, and a brown-grey, scoriaceous basaltic andesite containing ~5255 wt% SiO2 (Neill et al., 2015). Both lithologies are co-linear on many whole-rock elementelement variation diagrams, but significant differences in some elements and ratios indicate thatthe two magmas were petrogenetically distinct, and that pre-eruptive mixing between the two
was limited [4]. Groundmass glass compositions support this inference (Figure 1): at a given
SiO2 content, andesite glass compositions have significantly lower K2O concentrations andK2O/SiO2 ratios. Trends in SiO2 vs. TiO2 and vs. P2O5 may indicate separate evolution of theandesite and basaltic andesite, with only late mixing between the two magmatic components.
All melt inclusions and groundmass glass from both the andesite and basaltic andesite
record Cl concentrations of >1800 ppm, with the majority of concentrations >3000 ppm (Figure2). Chlorine compositions show no significant correlation with either S or any major or minoroxide. Also, while Cl concentrations in melt inclusions appear slightly, albeit systematically,
higher than those of the groundmass glass in the andesite, the range in melt inclusion andgroundmass glass Cl concentrations overlap substantially in the basaltic andesite, thus
magmatic ascent must have been sufficiently rapid for only minimal Cl loss via degassing totake place. By contrast, S concentrations in melt inclusions reach ~600 ppm in andesite melt
inclusions and ~700 ppm in basaltic andesite melt inclusions, while groundmass glass S
concentrations from both andesite and basaltic andesite samples are <250 ppm. This reflects
the lower solubility and more rapid degassing of S (relative to Cl) in silicic magmas.
References:
Ruppert et al., J. Geophys. Res. 116 (2011), pp. B00B07
Kristiansen et al., J. Geophys. Res.-Atm. 115 (2010), pp. D00L16
Waythomas et al., J. Geophys. Res. 115 (2010), pp. B00B05
Neill et al.. Am. Mineral. 100 (2015), pp. 722-737
43

Figures:

44

ISOTOPIC CONSTRAINTS ON VOLATILE CYCLING WITHIN THE ALEUTIAN
ARC
Taryn Lopez1, Tobias Fischer2, Andrea Rizzo3
1
University of Alaska Fairbanks, Geophysical Institute, Fairbanks, AK, U.S.A.
2
University of New Mexico, Albuquerque, NM, U.S.A.
3
Istituto Nazionale di Geofisica e Vulcanologia (INGV), Palermo, Italy
Volatiles are cycled between the Earth’s interior and the exosphere primarily throughthe processes of subduction and arc volcanism. Volatiles released from arc volcanoes canoriginate from three sources: the subducted slab, mantle wedge and crust, each of which has asomewhat characteristic isotopic signature. For most well-studied volcanic arcs the subductedslab has been identified as the primary volatile source. The Aleutian Arc is home to some of
the most poorly-studied volcanoes in the world, due to their remote location. For this reason,
volatile cycling within this region is currently poorly constrained. To add to its intrigue, theAleutian Arc is also known for significant along-strike variations in subduction features
including convergence angle and rate, and subducted sediment flux, that we suspect strongly
influence volatile cycling. The western portion of the Aleutian Arc in particular is known for
low subducted sediment fluxes [Kelemen et al., 2003] and oblique convergence angles [DeMets
et al., 1990], which we hypothesize results in its volatiles being sourced primarily from the
mantle. Here we present new measurements of carbon and helium isotopes from volcanic gas
emissions from four Western Aleutian volcanoes collected during a field expedition in
September 2015. We compare the isotopic compositions of volcanic gases measured from ourtarget volcanoes to the expected compositional ranges of the three potential volatile sources,
and present preliminary interpretations of volatile provenance for the Western Aleutian Arc
segment.
The volcanoes targeted in this study (from west to east) include: Kiska, Little Sitkin,
Gareloi and Kanaga. Because each volcano has a different degassing manifestation, not allmeasurements were possible at each volcano. At Kiska, Little Sitkin and Kanaga we collected
plume samples for analysis of δ13C-CO2; while at Little Sitkin, Gareloi and Kanaga we collected
fumarole samples for 3He/4He analyses, using the following methods. Plume gases were drawn
into a lockable syringe, transferred into Tedlar bags, and then analyzed for CO2 concentrationand δ13C-CO2 composition on board the Maritime Maid Research Vessel using a Thermo
Scientific Delta Ray Isotope Analyzer. Between five and 20 samples were collected from eachtarget volcano to ensure a variety of sample compositions reflecting mixtures between plumeand ambient air. Then linear mixing trends between δ13C-CO2 and 1/CO2 (ppmv) were used to
extrapolate to the volcanic δ13C-CO2 source following the methods of Chiodini et al. [2011] andRizzo et al. [2014]. More details of this method can be found in Fischer and Lopez [2016].
Fumarole gases for He isotopic analysis were directly sampled by inserting a Titanium tube
into the fumarolic vent and then connecting this tube to a copper tube, via silicon tubing. Oncethe sampling stream had thermally equilibrated with the fumarolic gases, the up-stream anddown-stream ends of the copper tube were crimped to preserve the samples. These samples
were then analyzed at the Noble Gas Isotope Laboratory at the Istituto Nazionale di Geofisicae Vulcanologia (INGV), Palermo, Italy. He concentration and isotope ratio were measured
using a Helix SFT-GVI mass spectrometer following the methods of Rizzo et al., [2015]. The
20
Ne concentration, used to recalculate 4He/20Ne and to correct the 3He/4He for atmosphericcontamination, was measured in a Helix MC plus-Thermo mass spectrometer. Extrapolated
δ13C-CO2 values of -5.1‰, -1.99‰, and -4.3‰ (in comparison to the reference PDB) are foundfor Kiska, Little Sitkin and Kanaga volcanoes, respectively (Fig. 1). The average measured
3
He/4He ratios, first corrected for air contamination and normalized to the same ratio in air
45

(Rc/RA), yield 7.02, 7.72, and 8.01 RA for Little Sitkin, Gareloi and Kanaga volcanoes,
respectively (Fig. 1). Considering that these values largely fall within the range of typicalmantle δ13C-CO2 and Rc/RA values of 6.5±2.5‰ and 8±1, respectively, we propose that the
mantle is the primary volatile source for these Western Aleutian volcanoes. The exception tothis trend is Little Sitkin, whose δ13C-CO2 is heavier than typical MORB, which could
potentially reflect a carbonate source and/or isotopic fractionation. Complete geochemical
analysis of the sampled gases is currently underway, which will help provide broader context
to test and refine the interpretations presented here.
Figure 1: Measured
δ13C-CO2(blacksymbols, left axis)
and
Rc/RA
(red
symbols, right axis)
isotopic compositions
for Western Aleutian
volcanoes, plotted bylongitude.
Typicalmantle C and He
isotopic compositions
are
shown
for
reference, in gray andred, respectively.

References:
DeMets, C., R. G. Gordon, D. F. Argus, and S. Stein (1990), Current plate motions, Geophysics
Journal International, 101, 425-478.
Chiodini, G., Caliro, S., Aiuppa, A., Avino, R., Granieri, D. and Moretti, R. (2011). First
13 12
C/ C isotopic characterisation of volcanic plume CO2, Bulletin of Volcanology, 73(5): 531-542.
Fischer, T.P. and T.M. Lopez (2016), First airborne samples of a volcanic plume for δ13C of
CO2 determinations, Geophysical Research Letters, 43, doi:10.1002/2016GL068499.
Kelemen, P. B., G. M. Yogodzinski, and D. W. Scholl (2003), Along-strike variations in the
Aleutian Island Arc: Genesis of high Mg# andesite and implications for continental
crust, Inside the Subduction Factory, Geophysical Monograph, 138, 223-276.
Rizzo, A.L., Jost, H.-J., Caracausi, A., Paonita, A., Liotta, M. and Martelli, M. (2014), Realtime measurements of the concentration and isotope composition of atmospheric andvolcanic CO2 at Mount Etna (Italy), Geophysical Research Letters, 41: 2382-2389.
Rizzo, A., F. Barberi, M.L. Carapezza, A. Di Piazza, L. Francalanci, F. Sortino and W.
D’Alessandro (2015), New mafic magma refilling a quiescent volcano: Evidence from
He-Ne-Ar isotopes during the 2011–2012 unrest at Santorini, Greece, Geochemistry
Geophysics Geosystems, doi:10.1002/2014GC005653.

46

LAHAR INUNDATION MODELING WITH THE AID OF HISTORIC FLOWDEPOSITS AT REDOUBT VOLCANO, COOK INLET, ALASKA
Alex M. Iezzi 1, 2, Douglas M. Thompson 2, Beverly Chomiak 2
1
Geophysical Institute, Alaska Volcano Observatory, University of Alaska Fairbanks
2
Department of Physics, Astronomy, and Geophysics, Connecticut College
Redoubt Volcano is a 3108 m tall stratocone located in Cook Inlet, Alaska that explosively
erupts roughly every 20 years. The five eruptions since 1900 all share the common
characteristic of being accompanied by multiple large to very large lahars (108 to 109 m3), as
well as many that are smaller in magnitude (104 to 106 m3). About 35 km from the crater ofRedoubt Volcano lies the Drift River Marine Terminal that, if inundated, has the potential tocause an oil spill comparable in size to the Exxon Valdez spill of 1989. Non-Newtonian lahar
flows evolve as they move down valley as a result of their bulking and debulking processes.
The aim of this project was to model the largest lahars from the three most recent eruptions ofRedoubt to better predict the area of inundation during future eruptions. Using GIS and thelahar simulation program Laharz_py, inundation models were created and compared with the
known mapped area of post-eruption inundation done by the USGS for the seven mostextensively studied lahars spanning the three most recent eruptions (1966-68, 1989-90, and2009). The input data for these simulations consisted of a ten-meter resolution DEM andestimates of glacial meltwater volume as a measure of initial lahar volume proposed by both
Dorava and Meyer (1994) and Waythomas et al. (2013). To capture the specific characteristicsof the Redoubt Volcano lahars, a retrospective manipulation of the calibration factors was
performed, such as the starting coordinates of the lahars, using the previously mapped areas ofinundation.
Dorava, J. M., & Meyer, D. F. (1994). Hydrologic hazards in the lower Drift River basinassociated with the 1989–1990 eruptions of Redoubt Volcano, Alaska. Journal ofVolcanology and Geothermal Research, 62 (1), 387-407.
Waythomas, C. F., Pierson, T. C., Major, J. J., & Scott, W. E. (2013). Voluminous ice-richand water-rich lahars generated during the 2009 eruption of Redoubt Volcano, Alaska.
Journal of Volcanology and Geothermal Research, 259, 389-413.

47

GEOLOGY AND 40AR/39AR GEOCHRONOLOGY OF LONG-LIVED AKUTAN
VOLCANO, EASTERN ALEUTIAN ISLANDS
Michelle Coombs1 and Brian Jicha2
1Volcano Science Center–Alaska Volcano Observatory, U.S. Geological Survey, Anchorage,
AK 99508, USA.
2
Department of Geoscience, University of Wisconsin, Madison, Wisconsin, 53706, USA.
40

Ar/39Ar dating and new whole-rock geochemical data expand the eruptive chronology
for Akutan volcano, Akutan Island, in the eastern Aleutian island arc. Akutan Island (166° W,
54.1° N) is the site of long-lived volcanism and the entire island comprises volcanic rocks as
old as 3.3 Ma (Richter et al., 1998, USGS Open-File 98-135). Our current focus is on the 225
km2 western half of the island, where the Holocene active cone, Holocene to latest Pleistocene
satellite vents, and underlying middle Pleistocene volcanic basement rocks are situated.
Eruptive products span the tholeiitic‒calc-alkaline boundary, are medium-K, and range frombasalt to dacite. Incremental heating experiments on groundmass separates of 69 samples
resulted in 55 40Ar/39Ar plateau ages. The oldest ages (2075±9 and 2323±40 ka) are from tworidges southeast of the Holocene cone; these likely represent the volcanic basement that
underlies the entire island. Above a major unconformity lie deeply eroded lavas from a several
older satellite vents/volcanoes including Open Bight (765–752 ka), Lava Peak (605–595 ka),and Long Valley (678–522 ka). Two younger eruptive centers, Flat Top (155–98 ka) andCascade Bight (63–43 ka) are located 3.5 km southwest and 4.5 km southeast of the current
cone. Akutan edifice spans the last 286 kyr and has had two Holocene caldera forming
eruptions. Our results show that the focus of volcanism has shifted within the western half of
Akutan Island over the last ~700 ka, and that on occasion, multiple volcanic centers have been
active over the same time period, including within the Holocene.
Holocene lavas, including those from Cascade Bight and Lava Point satellite vent on
the NW coast, all fall along a single tholeiitic, basalt-to-dacite evolutionary trend that has lower
K than Pleistocene lavas. Most “calc-alkaline” lavas show evidence consistent with theirformation by mixing of mafic and evolved rocks, not through crystallization-derived
differentiation through the calc-alkaline trend. Earliest lavas are mafic, have high La/Yb ratios
consistent with broadly dispersed low degrees of partial melting throughout the mantle wedge.
These magmas erupted prior to the development of Pleistocene fluctuations in glacial cover.
Similar magmas erupted from Flat Top during MIS5, a time of rapid glacial unloading.

48

PETROLOGIC CHRONOLOGY OF THE 1999 SUB-PLINIAN ERUPTION OF
SHISHALDIN VOLCANO
Daniel Rasmussen1, Terry Plank1, Amanda Lough2, Pete Stelling3, Diana Roman2
1Lamont-Doherty Earth Observatory of Columbia University, Palisades, NY, USA.
2
Department of Terrestrial Magnetism, Carnegie Institution of Washington, Washington, DC,USA.
3
Geology Department, Western Washington University, Bellingham, WA, USA.
On April 19, 1999 Shishaldin volcano burst to life, ejecting over 43 million cubic metersof basaltic ash into the atmosphere in a sub-Plinian eruption. InSAR images reveal a surprisinglack of deformation preceding or accompanying the VEI 3 eruption (Moran et al., 2006 JVGR).
Here we study olivine from this eruption to constrain subsurface magma movements andexplore the causes of this unusual behavior. One possibility is that deep (>10 km) magma
ascends relatively rapidly (i.e., within months) to shallow depths just prior to eruption (Moranet al., 2006 JVGR). This interpretation is consistent with the onset of long period seismic events
suggesting the initiation of upward magma migration from depths of >15 km as early as Julyof 1998 (Moran et al., 2002 BV). By early February of 1999, at least some magma had reachedthe near-surface, as evidenced by a remotely-sensed thermal anomaly in the summit crater andvigorous steam venting. We can test the proposed open-vent behavior by determining precise
locations of magmas and timing of pre-eruptive magmatic events (e.g., mixing) throughpetrologic analysis. This will serve both to inform our interpretation of precursory signals used
to evaluate volcanic risks and aid in our understanding of open-vent volcanism.
We investigate chemical zonation and melt inclusions in olivines from the 1999 ash.
Olivine core compositions are bimodal, with a broad mode centered on Fo62 and a much smaller
mode of more primitive compositions near Fo78. Most low-Fo olivines are reversely zoned,
whereas high-Fo olivine are normally zoned, which provides strong evidence of magma mixing.
The mixing-to-eruption timescale can be recovered from chemical gradients frozen in crystals
that are erupted during partial diffusive equilibration, following a mixing event. Preliminary
results of diffusion modeling suggest mixing occurred months to days prior to eruption. Such alarge range of timescales implies that recharge did not occur at a single point in time, rather it
was a prolonged event, which is consistent with seismic observations. Spatial constraints forthis process can be provided by the study of melt inclusions, which act as pressure gauges
because the dissolved volatile contents recorded by inclusions are strongly dependent on thepressures of entrapment. The majority of inclusions are found within the cores of low-Fo
olivines. These inclusions have low volatile contents (0.2-2.1 wt.% H2O, 0-164 ppm CO2) andlack vapor bubbles. Vapor saturation pressures suggest maximum entrapment depths of 2.7 km,
meaning the bulk of the more evolved mixing endmember was located within the edifice of
Shishaldin. A second population of melt inclusions are entrapped within the reversely zoned
rims of low-Fo olivine. These inclusions have higher volatile contents (0.6-2.4 wt.% H2O, 199330 ppm CO2) and contain vapor bubbles. Entrapment occurred at depths of at least 3.5 km,
which is likely to be consistent (after accounting for vapor bubbles) with the maximum depthof volcanic tremor at 5-6 km that occurred in the month leading up to the eruption (Thompson
et al., 2002 BV). Thus, olivines record a rich history of the eruption that may relate closely togeophysical observations and bear on the causes of open-vent volcanism.

49

SOURCING PREHISTORIC OBSIDIAN TOOLS IN THE ISLANDS OF FOUR
MOUNTAINS, ALASKASam H. Sheffer1, Virginia Hatfield2, Kirsten Nicolaysen1, Thomas Bartlett III3, Dixie
West2, Emily Deacon1, Kale Bruner2
1
Whitman College, Walla Walla, WA, USA.
2
Biodiversity Institute, University of Kansas, Lawrence, KS, USA.
3
Colgate University, Hamilton, NY, USA.
Unlike lavas and jaspers, obsidian possesses more homogeneous compositions
amenable to analysis by portable X-Ray Fluorescence (pXRF). Fractured obsidian producesthin, sharp edges ideal for knives and projectiles, though prehistoric Aleutians sites also include
tools made of conchoidally fracturing aphyric lavas and jasper/opal. In the Islands of the Four
Mountains (IFM), obsidian artifacts are found within cultural layers rich in datable organic
matter and interbedded with distinctive tephra deposits (Hatfield et al., 2016). Because it offers
rapid non-destructive analysis, pXRF is used to characterize and compare the chemicalsignatures of possible volcanic source materials available for tool-making and the tools
themselves. A comparison of the compositions of 121 artifact fragments reveals similarities anddifferences for lithic resource use among six sites on three of the Islands of Four Mountains.
The isolated, windswept islands of Chuginadak, Carlisle, and Herbert lie in thetransition from the eastern to the central Aleutian arc. Although these islands are currently
uninhabited, the Unangax (Aleut) lived here for millennia (e.g., Laughlin, 1963; McCartney,
1984; West et al., 1999; Dumond and Knecht, 2001). 14C dates of occupation by the IFM
research team span as far back as 3632-3724 calibrated years BP (100% probability, 2 ). In
2014 and 2015, obsidian artifacts especially tiny flakes or debitage (debris from making stone
tools) were recovered from three prehistoric sites on Chuginadak Island and two prehistoricsites on Carlisle Island. In Unit 4 within a Carlisle Island site, the stratigraphy revealed many
tools or tool fragments within multiple occupation horizons.
An investigation, using scatter plots of calibrated elemental data of obsidian identifies
a unique signature for most IFM obsidian artifacts. Three replicate analyses of each sample andinterspersed analytical standards produced accurate and precise measurements of elements Zr,
Zn, Ca, Pb, K, and Nb. Use of the obsidian standards SPHM-1 and GBO plus powdered GSP2, also provided calibration curves to correct the accuracy for precise elements Sr, Rb, Th, Fe,
Mn, Ti, Ba, Al, and Si. Trace element ratios show most IFM obsidian artifacts cluster atconsistent values such as Zr/Nb (24-26ppm), Fe/Mn (27-32ppm), and Ba/Rb (12-20ppm) showsthat prehistoric IFM occupants primarily utilized one obsidian source. The discovery of a single
lithic source suggests information sharing and cultural interaction among different IFM villages
and islands. Zr/Nb, Fe/Mn and Ba/Rb clusters are distinct from previously characterized
obsidian sources on Okmok and Akutan. However, one deeply buried artifact within a site on
Carlisle Island matches Okmok obsidian elemental signature. Additionally, artifacts collectedfrom Carlisle Island Unit 4 show that the same obsidian type was used consistently among
stratigraphically-related different cultural horizons, i.e., through time.

50THE RELATION BETWEEN PRE-FRAGMENTATION BUBBLE SIZE
DISTRIBUTION, ASH PARTICLE MORPHOLOGY, AND THEIR INTERNALDENSITY: IMPLICATIONS TO VOLCANIC ASH TRANSPORT ANDDISPERSION MODELS
Alexander Proussevitch1, Pavel Izbekov2, Dork Sahagian3
1
Earth Systems Research Center, University of New Hampshire, Durham, NH 03824, USA
2
Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK 99775, USA
3
Lehigh University, Bethlehem, PA 18015, USA
Parameterization of volcanic ash transport and dispersion (VATD) models strongly depends
on particle morphology and their internal properties. Shape of ash particles affects terminal
fall velocities (TFV) and, mostly, dispersion. Internal density combined with particle size hasa very strong impact on TFV and ultimately on the rate of ash cloud thinning and particle
sedimentation on the ground.
Unlike other parameters, internal density of vesicular ash particle cannot be measured directly
because of the micron scale sizes of fine ash particles and the presence of vesicles, but wedemonstrate that it varies greatly depending on the particle size. Small simple type ash particles(fragments of bubble walls, 5-20 micron size) do not contain whole large magmatic bubbles
inside and their internal density is almost the same as that of volcanic glass matrix. On the otherside, the larger compound type ash particles (>16 microns for silicic fine ashes) always containsome bubbles or the whole spectra of bubble size distribution (BSD), i.e. bubbles of all sizes,
bringing their internal density down as compared to simple ash. So, density of the larger ash
particles is a function of the void fraction inside them (magmatic bubbles) which, in turn, is
controlled by BSD. Volcanic ash is a product of the fragmentation of magmatic foam formedby pre-fragmentation bubble population and characterized by BSD. The latter can now bemeasured from bubble imprints on ash particle surfaces using stereo-scanning electron
microscopy (SSEM) and BubbleMaker software developed at UNH, or using traditional highresolution computed X-Ray tomography (HR-XCT).
In this work we present the mathematical and statistical formulation for this problem
connecting internal ash density with particle size and BSD, and demonstrate how the TFV of
the ash population is affected by variation of particle density.
Theoretical formulations have been preliminarily validated with direct particle density
measurements using Scanning Electron Microscope (SEM) and Back Scattered Electron(BSE) imagery analysis of particle cross-sections. We have used fine ash samples of explosive
eruptions of Augustine Volcano in 1986, Redoubt Volcano in 2009. Loose micron-scale ash
particle mounts have been mapped by SEM imagery, then impregnated in epoxy, polished,and examined using BSE analysis. The ratio of void to matrix area in individual ash particles
has been used to measure each particle density. Our results are consistent with the theoretically
predicted ash particle density distribution.

51

NEW DISCOVERED LATE MIOCENE VERCHNEAVACHINSKAY CALDERA ON
EASTERN KAMCHATKA (UPSTREAM OF LEVAYA AVACHA AND KAVYCHARIVERS): GEOLOGY, BOUNDARY AND COMPOSITION
O.V. Bergal-Kuvikas1,2, V.L. Leonov2, A.N. Rogozin2, I.N. Bindeman3, E.S. Kliapitskiy2
1
Earth Observatory of Singapore, Nanyang Technological University, Singapore
2
Institute of Volcanology and Seismology, Petropavlovsk-Kamchatsky, Russia
3
University of Oregon, USA
During 2009, 2010, 2014 field works the new obtained caldera complex descripted inspringheads of Levaya Avacha and Kavycha rivers (Eastern Range, Kamchatka) (Kuvikas &Rogozin, 2009; Leonov et al., 2011). Natural outcrops represented by thick interbedded layersof welded tuffs and ignimbrite (>500 meters thickness). The interbedded layers cover nearly 10
km area (Fig. 1). Volume of pyroclastic deposits was calculated as 220-230 km3, based on sizeof caldera (Mason et al., 2004). These ejected volumes correspond to strong explosive
eruptions with VEI 7 or more. The age of caldera-forming eruption was determined by Ar-Ar
method to be of Late Miocene (5.78~5.58 Ma BP).
Detailed descriptions of the numerous thin sections and whole-rock geochemistry
allows us to correlate sections of exposed outcrops from Verhneavachinskaya caldera (Fig. 2).
We distinguished four main types of the rocks, which are characterized by different major andtrace element composition, colors, textures, mineralogical and geochemical compositions. First
types of the layers is ignimbrite of basaltic andesitic composition. Columnar jointing occurs at
the most of the ignimbrite, exposed by active erosion process. Pyroclastic texture characterize
most ignimbrite layers: microtexture represents by fragments of plagioclase, pyroxene
phenocrystalls, and matrix of the rocks contains lithified welded tuffs with numerous fiammes.
Second type of the layers is black, dense basaltic andesite less-changed ignimbrite layers.
Structure of rocks contents fragments of plagioclase, pyroxene phenocrysts. Matrix of rocks
represents by oriented plagioclase microlites. Third type is altered tuffs with yellow-orange
tone. These rocks characterized by significant secondary hydrothermal alteration of rock`smatrix with quartz micro veins. Fourth type of the layers is volcanic breccias, which composedof broken different sizes rocks fragments with cemented tuffs matrix.
Whole-rock geochemistry of ignimbrite changes from basalt to andesite (SiO2 51.2-59.5
wt. %), with corresponding natural decreasing FeO*, CaO, MgO, TiO2. Across the outcrops
from lower to upper ignimbrite layers the decreasing contents of SiO2, MgO, Na2O are observedwith minimum on the top of outcrop. In comparing with another ignimbrite fields on Kamchatka
the rocks from Verhneavachinskaya caldera characterized by higher contents of Nb, Ta, TiO2
and MgO, lower contents of Na2O, SiO2 (Kliapitskiy, 2014).
New discovery of the Late Miocene Verhneavachinskaya caldera is as one of the older
and mafic complex on Kamchatka opens many questions for origin and evolution magma in
active island arc system: which are features of Late Miocene volcanism and how it correlatewith geodynamic setting, e.g. with slab jumping and originated transform faults (Avdeiko,Bergal-Kuvikas, 2015).
Reference
Avdeiko, Bergal-Kuvikas. The geodynamic conditions for the generation of adakites and Nb-rich basalts... JVS, 2015. 9(5),295-306.
Kliapitskiy. New data of geochemistry of ignimbrites…. XIII Regional young scientist conference. 2014. p. 81-90 p.
Kuvikas, Rogozin. First results of study 500-meters section...VII Regional conference for young scientists. 2009. p. 39-49.
Leonov et al. Determination of new caldera on Kamchatka… Material of conference to volcanologist day. 2011. 53-56 p.
Mason et al. The size and frequency of the largest explosive eruptions on Earth. Bull. Volcanol. 2004. V.66. p. 735-748.

52

Fig. 1 a) General plate tectonic
position of the Kamchatka andlocation of the Verhneavachinskaya
caldera (black square).
b) Scheme of geological structure of springheads of Levaya Avacha and Kavycha rivers (Leonov et al.,2011). Note: 1 - Late Pleistocene-Holocene alluvium, glacial and debris deposits, arrows indicate
movement of landslides, 2 - Pleistocene cinder comes and related lava flows, 3 – Pliocene-Early
Pleistocene andesitic lava flows, 4 – Late Miocene ignimbrite deposits, 5 – Latter Miocene diorite
intrusions, 6 – Miocene porphyritic basalts, agglomerate tuff, 7 - Late Cretaceous siltstones, argillites,
8 – cliffs of Avachinsky range, 9 - faults which are boundary graben of Srednyaya Avacha river, 10 boundary of new-discovered caldera, 11- location of studied outcrops of ignimbrites (1-L-2010, 2-L2014, 3-L-2012, 4- R-2009, 5-L-2009, please see details on Fig. 2), 12 – dip of the ignimbrite layer.

Fig. 2. Correlation ofstratigraphic sections. Note: 1ignimbrite layers, 2- marked
ignimbrite layers, which arecorrelated on the sections, 3altered tuffs with yellow-orange
tones, 4-volcanic breccia, 5numbers of the section are
showed on Fig. 1, 6 – sodded
outcrop area.

53

ALASKA TEPHRA DATABASE
Cheryl Cameron1, Katherine Mulliken1, Janet Schaefer1, Kristi Wallace2, Scott Crass1
1
Alaska Division of Geological & Geophysical Surveys, Fairbanks AK.
2
U.S. Geological Survey, Anchorage AK.
The Alaska Volcano Observatory (AVO) began construction of an Alaska tephra (volcanicash) database in 2014. This project is a joint effort between staff at the Alaska Division of
Geological & Geophysical Surveys (DGGS) and the USGS Alaska Tephra Lab. The Alaska
tephra database houses all pertinent information on Alaska tephras, necessary for sample
processing, archiving, and scientific research, and is fully integrated within AVO’s larger
Geologic Database of Information on Volcanoes in Alaska (GeoDIVA).
Tephra studies are a key component in understanding the process, magnitude, and frequencyof volcanic eruptions, and improve volcanic ashfall hazard assessments and ashfall modeling
efforts. Tephrostratigraphy is an integral part of linking marine, lacustrine, and terrestrial
records critical to research of paleoclimate and archaeology. Developing correlations of tephra
records across Alaska and the northern hemisphere requires an understanding of the age,chemistry, and character of tephra deposits. Currently, chemical, stratigraphic, and age data for
Alaska tephra are dispersed in hundreds of publications and unpublished lab results, making
efficient querying of data for specific research purposes impossible.
Our tephra database, with its associated web portals, will strive to alleviate this difficulty
and make Alaska tephra data easily accessible for scientists. We are constructing the databasein stages. The current database population and query focus is: basic sample information, sample
age, and calculated averages from electron microprobe (EMPA) chemical analyses of glass. We
have prioritized key marker-horizon tephras and have now entered sample information and
EMPA glass averages for nearly 1,900 samples across Alaska, including those from Aniakchakand Hayes volcanoes, the Ahklun mountains area, Dawson tephra, Sheep Creek tephra, Old
Crow tephra, and the White River Ash. We are about halfway through the available publisheddata for EMPA glass averages from Alaska tephra.
We have also built an internal web portal to query sample metadata and geochemical databy geologist, author, publication, location, or known source volcano. After retrievinggeochemical results a user may calculate a correlation coefficient using their desired
parameters.
For the next phase, we plan improvements to the web portal, including search by possible
source volcano, age, and spatial map query as well as improvements to the output to include
number of analyses, standard deviation, and standards used in the analysis. When the web portal
is robust, it will become available on the AVO public website.
Further steps to expand tephra data stored in the database include storing sample processing
details and individual grain-point and mineral analyses as well as creating a laboratory interface
for post-field sample workflow. We welcome feedback, comments, and questions frompotential database users or dataset contributors.

54

PETROLOGY AND GEOCHEMISTRY OF THREE EARLY HOLOCENEERUPTIONS FROM MAKUSHIN VOLCANO, ALASKA
Jessica F. Larsen1, Janet R. Schaefer2, James W. Vallance3
1
Geophysical Institute, Alaska Volcano Observatory, Univ. of Alaska. Fairbanks, AK, USA.
2
Alaska Division of Geological and Geophysical Surveys, Fairbanks, AK, USA.
3
U.S. Geological Survey, Cascades Volcano Observatory, Vancouver, WA, USA.
Makushin volcano is a XX m stratovolcano with ice-filled caldera/crater, located 25 km
west of Dutch Harbor and Unalaska village, Unalaska Island, Alaska. Makushin has producedon average one VEI 2-4 eruption every 200 years in the past 5000 C14 years (Bean, 1999).
Tephra fall deposits exist in and around the Dutch Harbor/Unalaska area, with individual layer
thicknesses from < 1 to ~20 cm locally. The three largest, most explosive Holocene eruptions
from Makushin occurred within a ~1000-year time period: “CFE”, (median radiocarbon age of9048 BP), “Nateekin” (8743 BP), and “Driftwood” (8198 BP). The CFE unit produced thickscoria fall deposits to the northeast and east of the volcano and pyroclastic flow deposits inupper Makushin and “Waterfall” valleys to the east and north. The Nateekin eruption produced
finer grained (fine ash to fine lapilli) deposits that are up to 20 cm in the Unalaska town area.
The Driftwood eruption produced thick tan pumice and dense, black scoriaceous fall deposits
primarily in the Driftwood valley and Lava Ramp area on the northeast flanks of the volcano.
Whole rock major and trace element compositions of 40 samples from the CFE andDriftwood eruptions were collected using XRF and LA-ICPMS analyses through the
Washington State University Geoanalytical Lab. Samples from the Nateekin unit were notanalyzed for whole rock geochemistry because they are too fine grained (typically <1cm lapilli
to fine ash). Electron probe microanalyses of glass, phenocryst, and microlite phases from all
three units were collected at UAF using the JEOL XX field emission electron microcprobe,
using standard conditions for glass and mineral phases.
The CFE and Driftwood eruptions produced medium K2O, tholeiitic (Miyashiro, 1974)
andesites: CFE = 56 to 60 wt. % SiO2; Driftwood = 60 to 63 wt. % SiO2. The three units haveandesite to rhyodacite glass compositions, as follows: CFE= 57 to 64 wt. % SiO2; Nateekin =59 to 61 wt. % SiO2; Driftwood = 67 to 70 wt. % SiO2. The CFE and Driftwood scoria andpumice samples have plagioclase, clinopyroxene and orthopyroxene as the primary mineralphases, with minor olivine in the CFE fall deposit scoria. The pyroxenes in the CFE andDriftwood samples are uniform in composition with orthopyroxenes = Wo4.6En58.7Fs36.7 (n=58)
and clinopyroxenes = Wo39.7En41.9Fs18.4 (n=132). Plagioclase phenocrysts from Driftwood
pumice have An52-54 cores and slightly more sodic rims of An48-49. CFE plagioclase phenocrysts
are not as uniform, with a lower An50-54 group and a higher An70-89 group.
The Nateekin glass compositions are very similar to those from CFE scoria samples
from the middle to top of the unit. Thus, the Nateekin eruption may have tapped the same
magma body as the CFE, indicating the magma system did not change significantly in the ~300year time period between the two eruptions. The Driftwood eruption produced an andesite withhigher SiO2, Al2O3, FeO, and lower MgO magma than the CFE. It is unlikely to be related to
the CFE magma by simple fractionation of pyroxenes and plagioclase, indicating a significant
change in the magma stored beneath Makushin in the ~700 years between the Nateekin andDriftwood eruptions.

55

INTERDISCIPLINARY POSTER SESSION(Abstracts are listed sequentially according to the
Scientific Program)

56

FULL MOMENT TENSOR AND SOURCE-TYPE ESTIMATION FOR VOLCANICEVENTS
Celso R. Alvizuri, Carl Tape
Geophysical Institute and Department of Geosciences, Univ. of Alaska Fairbanks, Fairbanks,
AlaskaThe seismic full moment tensor is a general representation of any seismic point source, and canrepresent double-couple (DC) but also non-DC mechanisms such as isotropic and CLVD. We
present a catalog of full seismic moment tensors for 63 small (Mw < 3) events from Uturuncu
volcano in Bolivia. The events were recorded by up to 24 broadband stations during an array
deployment by the PLUTONS project between 2010-2012. Most events had magnitudes
between 0.5 < Mw < 2.0 and did not generate discernible surface waves. We estimate each
event from a grid-search over the six-dimensional space of moment tensors. For each event wecomputed the misfit between observed and synthetic waveforms, and we also used first- motion
polarity measurements to reduce the number of possible solutions. Each moment tensor solution
was obtained using a grid search over the six-dimensional space of moment tensors. For each
event we characterize the variation of moment tensor source type by plotting the misfit functionin eigenvalue space, represented by a lune. We identify three main types of events in the catalog:(1) 6 isotropic events, (2) 5 tensional crack events, and (3) a swarm of 14 events that appear to
be double-couples. The occurrence of positively isotropic events is consistent with otherpublished results from volcanic and geothermal regions. Several of these previous results, aswell as our results, cannot be interpreted within the context of either an oblique opening crack
or a crack-plus-double-couple model; instead they require a multiple-process source model.
Our study emphasizes the importance of characterizing uncertainties for full moment tensors,and it provides strong support for isotropic events at Uturuncu volcano.

57

GENERATING DYNAMIC VOLCANIC HAZARD MAPS FOR DOMINICA, LESSERANTILLES BY USING GEOPHYSICAL DATA AS WEIGHTS IN SPATIALINTENSITY MAPS
Ophelia George1, Joan L. Latchman2, Charles Connor1, Stephen McNutt1, Laura
Connor1
1
School of Geosciences, University of South Florida, Tampa, Florida, 33620
2
Seismic Research Center, University of the West Indies, Port of Spain, Trinidad, West Indies
Risk posed by volcanic eruptions are generally quantified in a few ways; in the shortterm geophysical data such as seismic activity or ground deformation are used to assess thestate of volcanic unrest while statistical approaches such as spatial density estimates are used
for long term hazard assessment. Spatial density estimates have been used in a number ofmonogenetic volcanic fields for hazard map generation and utilize the age, location andvolumes of previous eruptions to calculate the probability of a new event occurring at a given
location within this field. In a previously unpublished study, spatial density estimates of theLesser Antilles volcanic arc showed the island of Dominica to have the highest likelihood of
future vent formation. In this current study, this technique was used in combination with the
SRC catalog of seismic events occurring beneath Dominica within the last ~ 20 years togenerate a hazard map which not only takes into consideration the past events but also thecurrent state of unrest. Here, geophysical data serve as a weighting factor in the estimates withthose centers showing more vigorous activity receiving stronger favorability in the assessment
for future activity. In addition to this weighting, the bandwidth utilized in the 2D-ellipticalkernel density function was optimized using the SAMSE method so as to find the value which
best minimizes the error in the estimate. The end results of this study are dynamic volcanic
hazards maps which will be readily updatable as changes in the geophysical data occur.

58

GEOMECHANICAL INTERPRETATION OF LOCAL SEISMICITY CONCERNINGACTIVITY OF TOLBACHIK, KORYAKSKY AND AVACHINSKY VOLCANOESOF KAMCHATKA IN 2008-2012
A.V. Kiryukhin, S.A. Fedotov, P.A. Kiryukhin
Institute of Volcanology & Seismology FEB RAS, Piip 9, P-Kamchatskii, Russia, 683006
Exigen Services, Pulkovskoe 40-1, Saint-Petersburg, Russia, 196158
Local seismic activity during 2012 eruption of Tolbachik volcano and 2008-2009 steamgas eruption of Koryaksky volcano is considered as a result of the injection of magma forming
plane-oriented zones: dykes, sills and activation of existing faults. To identify these zones theplane-oriented clusters of earthquakes were distinguished with the catalogs of Kamchatka
Branch of Geophysical Survey RAS, their subsequent spatial-temporal analysis allows thefollowing interpretation. 27.11.2012. Tolbachik volcano eruption was preceded by the injectionof magma with the introduction of a series of dikes of west-north-west striking in the depth
range -4 - +3 km abs. in the area to the southeast of the Plosky Tolbachik volcano. The indicatedfractures dissection of a subhorizontal permeable zone at an altitude near zero lead to theformation of sills and magma discharge injection dike (dip angle of 50°, dip azimuth 300о) at
5.5 km from the epicenter of the initial magma injection. 2008-2009 summit steam-gas eruptionof Koryaksky volcano was preceded by the crustal chamber being saturated with magma (thedepth of the roof -3 km abs, width 2.5 km) at the south-western foot of the Koryak volcano,further injection of magma in submeridional area (7.5 x 2.5 km, depth range -2 - -5 km abs.) of
the northern sector of Koryaksky volcano occurred in parallel with the summit steam-gas
eruption. The injection of magma into the cone of Avacha volcano (2010) took place with thecone being saturated with sills (in the range of marks +1600 - +1900 masl) and dikes (mostly
of NW-trending).

59

SEISMIC MOMENT TENSORS AND ESTIMATED UNCERTAINTIES IN
SOUTHERN ALASKA SUBDUCTION ZONE
Vipul Silwal and Carl Tape
Department of Geosciences, University of Alaska Fairbanks, Alaska, USA
We present a moment tensor catalog of 106 earthquakes in southern Alaska, and we perform aconceptually based uncertainty analysis for 21 of them. For each earthquake, we use both bodywaves and surface waves to do a grid search over double couple moment tensors and source
depths. For smaller events we also include the first-motion polarity information to further
constrain the solution. The combination of waveform and polarity misfit gives the total misfit
function, at the minimum of which lies the solution. For our purposes, the inclusion of polarity
misfit proved immensely beneficial when performing source inversion of small events around
Cook Inlet and could possibly help in delineating unknown faults. The uncertainty parameteror, rather, our confidence parameter is the average value of the curve P(V), where P(V) is theposterior probability as a function of the fractional volume V of moment tensor spacesurrounding the minimum-misfit moment tensor. As a supplemental means for characterizing
and visualizing uncertainties, we generate moment tensor samples of the posterior probability.
We perform a series of inversion tests to quantify the impact of certain decisions made within
moment tensor inversions and to make comparisons with existing catalogs. For example, using
an L1 norm in the misfit function provides more reliable solutions than an L2 norm, especiallyin cases when all available waveforms are used. Using body waves in addition to surface waves,as well as using more stations, leads to the most accurate moment tensor solutions. These
choices will be important when implementing real-time moment tensor inversion in Alaska.
Our estimation of uncertainties will be important for identifying the style of faulting within yetto-be-discovered fault zones.

60

TRACKING GLACIERS WITH THE ALASKA SEISMIC NETWORK
Michael West1, Natalia Ruppert1, Natalia Kozyreva1, Sara Meyer1, Dara Merz1, Miriam
Braun1
1
Alaska Earthquake Center, Geophys. Institute, Univ. Alaska Fairbanks, Fairbanks, AK, USA.
More than 40 years ago it was known that calving glaciers in Alaska created unmistakableseismic signals that could be recorded tens and hundreds of kilometers away. Their longmonochromatic signals invited studies that foreshadowed the more recent surge in glacierseismology. Beyond a handful of targeted studies, these signals have remained a seismic
novelty. No systematic attempt has been made to catalog and track glacier seismicity across theyears. Recent advances in understanding glacier sources, combined with the climate
significance of tidewater glaciers, have renewed calls for comprehensive tracking of glacierseismicity in coastal Alaska. The Alaska Earthquake Center has included glacier events in its
production earthquake catalog for decades. Until recently, these were best thought of as
bycatch—accidental finds in the process of tracking earthquakes. Processing improvements a
decade ago, combined with network improvements in the past five years, have turned this intoa rich data stream capturing hundreds of events per year across 600 km of the coastal mountain
range. Though the source of these signals is generally found to be iceberg calving, there arevast differences in behavior between different glacier termini. Some glaciers have strong peaksin activity during the spring, while others peak in the late summer or fall. These patterns are
consistent over years pointing to fundamental differences in calving behavior. In several cases,changes in seismic activity correspond to specific process changes observed through othermeans at particular glacier. These observations demonstrate that the current network isproviding a faithful record of the dynamic behavior of several glaciers in coastal Alaska. With
this as a starting point, we examine what is possible (and not possible) going forward withdedicated detection schemes.

61

LONG-TERM OCEAN BOTTOM MONITORING OF SLOW EARTHQUAKES ON
THE SHALLOW PLATE INTERFACE IN HYUGA-NADA, WESTERN PART OF
THE NANKAI TROUGH
Yusuke Yamashita1, Masanao Shinohara2, Tomoaki Yamada2, Kazuo Nakahigashi3 ,Hajime Shiobara2, Kimihiro Mochizuki2, Takuto Maeda2, Kazushige Obara2
1
Miyazaki Obs. Disaster Prevention Research Institute (DPRI), Kyoto University, Japan.
2
Earthquake Research Institute (ERI), the Univ. of Tokyo, Japan.
3
Tokyo University of Marine Science and Technology, Japan.
The Hyuga-nada region, western part of the Nankai Trough in Japan, is one of the mostactive areas of shallow slow earthquakes in the world. Recently, ocean-bottom observation of
offshore seismicity near the trench have succeeded to detect shallow tremor as a complete
episode lasting for one month exhibiting similar migration property of deep tremor for the firsttime [Yamashita et al., 2015 Science]. This activity was also associated with shallow very-lowfrequency earthquake (VLFE) activity documented by land-based broadband seismic network.
The coincidence between tremor and VLFE and their migration pattern show strong
resemblance with deep tremors during ETS episodes; this similarity suggests that the tremor
activity in the shallow plate boundary may also be coupled with VLFE and short-term slow slip
events (SSEs) in this area. However, the shallow SSEs have not been detected to date, probably
due to the lack of dense broadband seismic and/or geodetic observations in offshore. To clarify
the relationship among these slow earthquakes is important to improve the assessments of thepotential of tsunamigenic megathrust earthquake that is anticipated to occur at the Nankai
Trough.
Motivated by these issues, we have started long-term ocean-bottom monitoring of themin this area from May 2014 using three kinds of sensors: broadband seismometer with pressuregauge (BBOBSP) and short-period seismometer (LTOBS). This project is the first of the longterm continuous observation over several years in this area. During the first observation (March2014 to January 2015), minor shallow tremor and VLFE activity occurred just under the OBS
network. In addition, we confirmed that seismicity of ordinary earthquake was very low within
the focal area of shallow slow earthquake. The second observation started from January 2015
using 3 BBOBSPs and 10 LTOBSs, and all sensors were retrieved in January 2016. From themonitoring using land-based seismic observation, many shallow tremors and VLFEs occurredjust under the OBS network during second observation period, which started from early in May
2015 and continued approximately 2 months. We confirmed the existence of these signals inthe data recorded by each OBSs. Although the source locations are still not located, they were
probably migrated within the OBS network, which reached at off Cape Ashizuri area whereshallow VLFEs have been occurred every 6-7 years associated with long-term SSE at Bungo
channel. This off Cape Ashizuri’s activity (tremor and VLFE) started at the end of May,
especially increased activity after the large deep-focused earthquake at Ogasawara region(Mw7.8, 30 May 2015).
In the presentation, we will introduce the review of shallow slow earthquake
observation in Hyuga-nada and preliminary result of second observation, in particular focus on
the migration of shallow tremor.

62

GRAVITY DECREASE AND VOLCANIC INFLATION AROUND THE ACTIVE
CRATER AT TOKACHI-DAKE VOLCANO, HOKKAIDO, JAPAN
Noritoshi Okazaki1, Ryo Takahashi1, Makoto Tamura1, Hiroaki Takahashi2, Masayoshi
Ichiyanagi2, Teruhiro Yamaguchi2, Ryo Honda3, Yosuke Miyagi4, Akimichi Takagi5
1
Geological Survey of Hokkaido, Hokkaido Research Organization, Sapporo, Japan.
2
Institute of Seismology and Volcanology, Hokkaido University, Sapporo, Japan.
3
Tono Research Institute of Earthquake Science, Mizunami, Japan.
4
National Research Institute for Earth Science and Disaster Prevention, Tsukuba, Japan.
5
Meteorological Research Institute, Japan Meteorological Agency, Tsukuba, Japan.
Magmatic mass monitoring is one of fundamental parameter for activity forecasting.
Recent development in portable gravity meter and high precision GPS positioning techniques
have allowed us to make gravity observation on active volcano repeatedly. Simultaneous
observation of gravity and ground deformation at same point will provide valuable information
for deformation source material, e.g. magma or water.
Tokachi-dake volcano is one of the most active volcano in southwestern Kuril
subduction zone. Three magmatic eruptions had been recorded in a recent hundred years. We
installed the continuous GPS station in 2003 near the active crater in order to observe the grounddeformation that associated with the active volcanic activity. The local inflation continues
around the active crater from 2006. In order to investigate the cause of the inflation, we started
the relative microgravity measurement at 27 benchmarks from 2008. Scintrex CG-3M and CG5 gravity-meters, and dual-frequency GPS receiver for three dimensional positioning has been
simultaneously in operation at benchmarks.
Figure shows 5 results of the relative gravity measurement using GSH’s CG-5 from2010 to 2015. The gravity change is a tendency to decrease at active crater area, and reaches 0.12 to -0.14 mGal in 2015. On the other hand, the ground uplift in our GPS station (G016)
reaches a maximum of 0.2 m. Assuming a free air gradient (-0.3086mGal/m), if the ground is
0.2 m uplift, the gravity value is decreased by -0.062 mGal. Even includes measurement errors,
the gravity decreasecannot be explained only
ground uplift. Excessive
decrease of such gravity
values for ground uplift
has also been observed in
the Izu-Oshima volcano(Takagi et al., 2010). In
order to explain thisexcessive decrease, it isnecessary to consider suchas the changes in thedensity structure in theshallower part of under
the active crater.

63

THE KLUCHEVSKAYA VOLCANO GROUP OBSERVATION NETWORK 20062016. RUSSIA, KAMCHATKA.
S.S. Serovetnikov1, E.I. Gordeev2, Hiroaki Takahashi3, Pavel Izbekov4
1

Kamchatka Branch Geophysical Service, (KBGS RAS, Russia) sssu@emsd.ru
Science Institute of Volcanology and Seismology (IVS FEB RAS, Russia) aifgf@mail.ru
3
Hokkaido University (Japan) hiroaki@mail.sci.hokudai.ac.jp
4Geophysical Institute, UAF (USA) peizbekov@alaska.edu
2

Last 10 years of the Russian and international projects was actively developed the
networks of continuous geodynamic observations in various local parts of the Kluchevskoy
volcanic center. As a result, in 2011 was generated the geodynamic network over all
Kluchevskaya volcano group. The constant geodynamic stations of local observations overseparate volcanoes, was unite to Kluchevskaya volcano group observation network. Further the
network is extended constantly.
During the observations (2006-2016) have been registered the deformation processes
caused by activity volcanoes Bezimianny, Kuchevskoy and Tolbachik. Now the geodynamic
observations network includes 12 GNSS continuous stations, 5 Tiltmeter points and more than
50 points for periodic GNSS observations.
The Kluchevskaya volcano group observation network is created as a work result by
projects “PIRE” (2006-2010) – Geophysical Institute (UAF,USA), “KAKENY” (2010-2015) –Hokkaido University (Japan), (2013-2015) the Russian fund of basic researches (RFBR RAS
Russia), with assistance of Science Institute of Volcanology and Seismology (IVS FEB RAS,
Russia) and Kamchatka Branch Geophysical Service, (KBGS RAS, Russia).
The poster describes formation stages of the geodynamic Kluchevskaya volcano groupobservation network, some results of observations and the further prospects of observation
system development.

64

HAVE THE POSTSEISMIC MOTIONS DUE TO THE MAY 24, 2013 Mw 8.3
OKHOTSK DEEP FOCUS EARTHQUAKE BEEN DISCOVERED BY THE RUSSIANFAR EAST GNSS NETWORKS?
Nikolay Shestakov1,2, Grigory Nechaev1,2, Nikolay Titkov3, Mikhail Gerasimenko1,2,Victor Bykov4, Victor Pupatenko4, Sergey Serovetnikov3, Alexander Prytkov5, Nikolay
Vasilenko5, Dmitry Sysoev1,2, Alexey Sorokin6, Hiroaki Takahashi7 and Mako Ohzono7
1
Institute for Applied Mathematics of FEB RAS, Vladivostok, Russia
2
Far Eastern Federal University, Vladivostok, Russia
3
Kamchatka Branch of Geophysical Survey of RAS, Petropavlovsk-Kamchatsky, Russia
4
Institute of Tectonics and Geophysics of FEB RAS, Khabarovsk, Russia
5Institute of Marine Geology and Geophysics of FEB RAS, Yuzhno-Sakhalinsk, Russia
6Computing Center FEB RAS, Khabarovsk, Russia
7
Institute of Seismology and Volcanology, Hokkaido University, Sapporo, Japan
Three years have almost elapsed since the mainshock of the Okhotsk deep focus
earthquake occurred on May 24, 2013, at 05:45 UTC in the Sea of Okhotsk near the western
coast of the Kamchatka Peninsula. Up to now this seismic event has been remaining the largest
deep focus earthquake (Mw = 8.3) in the history of instrumental seismology. The earthquake
caused notable and measurable by GNSS technique 3-D coseismic crustal displacements in awide region around the epicenter. The detected offsets were used by several authors to develop
the earthquake source dislocation models. However, despite a significant number of measured
coseismic displacements and available a-priory seismological information, the parameters ofthese models have not been reliably determined.
In this work we analyze coordinate time series of a set of continuous geodetic sites thatbelong to different geodynamic GNSS networks deployed in the Kamchatka Peninsula,
Sakhalin Island and the western coastal areas of the Sea of Okhotsk and the Sea of Japan. The
considered time span covers 5 years before and almost 3 years after the earthquake (2008-2015).
We have discovered an abrupt annual velocity change after the mainshock at a set of GNSS
sites located within the above mentioned region. A coincidence of the beginning of the observed
effect with the time of the Okhotsk earthquake occurrence allows us to treat it as a consequenceof the earthquake. For most of the network stations, an increase of the western velocity
component by 1-4 mm/yr has been observed. Changes in the vertical GNSS site velocities havealso been detected, but their quantification is difficult due to limited accuracy of the verticaldisplacement measurements by GNSS technique. It should be noted that almost all of theobtained postseismic time series retain their linear behavior in contrast to the known examplesof postseismic time series caused by shallow earthquakes. Probably, the discussed annual
velocity changes detected after the deep focus earthquake have been obtained for the first time.
The physical mechanism of the observed phenomenon has not been clearly determinedyet. The deep (> 600 km) location of the Okhotsk earthquake hypocenter precludes us fromconsidering the poroelastic rebound mechanism as a possible candidate to explain the observed
effects. The afterslip impact on the observed surface displacements should also be small andrather rapidly decreasing with time. The viscoelastic relaxation and/or some other geodynamic
processes seem to provide a more appropriate explanation of the long-term annual velocitychanges which are observed in the Russian Far East after the Okhotsk earthquake.
This work was partially supported by FEFU grant No. 14-08-01-05_m and RFBR grantNo. 15-37-20269.

65

COMPOSITIONAL TRENDS OF АMPHIBOLE IN 2001-2013 YOUNG SHIVELUCH
ANDESITES AS EVIDENCE OF MAGMA CHAMBER REPLENISHMENT AND
SUBSEQUENT CONVECTION
Natalia Gorbach1, Maxim Portnyagin2,3, Tatiana Philosofova1
1
Institute of Volcanology and Seismology FED RAS, Petropavlovsk-Kamchatsky, Russia,
n_gorbach@mail.ru
2
GEOMAR Helmholtz Centre for Ocean Research Kiel, Kiel, Germany
3
V.I.Vernadsky Institute of Geochemistry and Analytical Chemistry RAS, Moscow, Russia
Hornblende-plagioclase andesites of the Young Shiveluch volcano erupted from 2001
to 2013 show minor variations of whole rock and matrix glass compositions but large variationsof mineral phenocryst compositions. We focused this work on the composition of amphiboles
in andesites from the growing Shiveluch lava dome, pumiсeous rocks from pyroclastic flows
and rare mafic inclusions. We propose that the shallow magma chamber was replenished during
this time that enhances magma convection and caused more frequent eruptions.
2001-2013 eruptive dynamics and whole rocks compositional variations
Intensive growth of the lava dome alternating with episodes of its destruction wasobserved in 2001-2013. During this period Young Shiveluch had five paroxysmal explosive
eruptions (May 2001 and May 2004, February and September 2005 and in October 2010). In
the course of these eruptions extensive pyroclastic flows covered the valleys on the southern
volcano slopes at a distance of 20-25 km from the eruptive center. In 2007, 2008, 2009 and2013 more moderate explosions also occurred and were accompanied of small-volume
pyroclastic flows. The volume of material erupted during 2001 - 2012 appears to be close to
0.8 km3 (Shevchenko et al., 2015) even if lavas erupted in 2013 and tephra placed outside of
the volcanic edifice are not taken into account.
SiO2 content in lava dome samples and pumice fragments from pyroclastic flows is60.5–64.0 wt.% and varies unsystematically over time. The andesites contains 15-20 to 45
vol.% phenocrysts which are represented by plagioclase with An in cores ranging from 30 to
83-88 mol. %, low- and high-Al amphiboles, and rare orthopyroxene and clinopyroxene with
Mg# 69-74. Rare olivine (Fo80-88) with reaction rim of orthopyroxene, Fe-Ti oxides andamphibole are presents in most samples. Groundmass is composed by plagioclase, subordinate
pyroxene, magnetite and rare amphibole microliths. Matrix glasses are rhyolitic (SiO2 =74 - 80wt.%) in all samples. Mafic inclusions, which were found in a block in pyroclastic deposits of2005 eruption (Gorbach, 2006) are olivine-hornblende basaltic andesite (SiO2 = 56.3 wt. %).
Amphibole texture and chemistry
Phenocrysts, microphenocrysts and rare microliths of amphiboles in the 2001-2013
eruptive products show a wide range of major element compositions (in wt.%: SiO2=40.4650.13; TiO2=0.56-3.54, Al2O3=6.18-14.06, FeO*=6.07-15.24, MgO=11.56-19.31, СaO=10.6212.59, Na2O=1.19-3.67, K2O=0.09-0.75). This compositional range corresponds tomasnesiohornblende (Mg-Hbl), pargasitic (Prg) and magnesiogastingsitic (Mg-Hst) amphibole
after Leake et al. (1997). Most crystals are idiomorphic. Opacitized amphiboles are rare in
2001-2013 andesites. Two main amphibole generations have been distinguished on the basis of
their textural and chemical features: 1) Middle-sized phenocrysts of Mg-Hbl (≥1-1.2 мм) withsimple chemical zoning (Al, Fe, Na decrease, Si and Mg increase from core to rim); 2) Large
phenocrysts (≥1.5-2 mm) with patchy, chemically very heterogeneous, especially with regard
to Al and Mg, core compositions containing abundant inclusions of melt, plagioclase andmagnetite. In addition to these generations, subphenocrysts (0.3-0.5 mm) and microlites (0.10.2 mm) of Prg and Mg-Hst hornblende were found in some samples erupted in 2004, 2007 and66

2013. Amphiboles phenocrysts and microliths from mafic inclusions correspond mainly to MgHst composition.
The most of zoned phenocrysts studied exhibit inverse correlation between Mg, Si (onthe one side) and Al, Ti, Fe, Na (on the other side), corresponding to edenite - Al-tschermakite
substitution. However, this correlation is disrupted in some crystals. For example, simultaneous
increase of Al and Mg is observed in amphiboles from mafic inclusions and on the crystal rims
at the contact of a host andesite with the inclusion, in some crystals from 2001, 2004, 2007 and2013 eruptions. The positive trend of Al and Mg (or of AlIV and Mg#, Fig.1) is interpreted in aseries of papers as trend magma replenishment (e.g., Sato et al, 2005; Kiss et al., 2014).
Fig. 1. AlIV (a.p.f.u.) vs. Mg# variations inamphiboles from 2001-2013 Young Shiveluch
rocks.
In result of mafic magma replenishment, the silica
content in magma decreases that leads to increasing
AlIV values in amphiboles. Mafic input also
increases Mg/Mg+Fe2+ ratio in the mixed magma.
Thus, simultaneous increase in AlIV and Mg# ofamphibole is expected to reflect magma
replenishment (Kiss et al., 2014).

Dirksen et al. (2006) proposed on the basis of olivine reaction rim study that mafic
replenishment preceded two months to four years the 2001 eruption. The data on amphibole
compositions are consistent with this conclusion and indicate that a part of the crystals ofamphiboles from 2001-2013 Young Shiveluch andesites crystallized from hotter magma.
According to Ridolfi et al. (2010) and Holland, Blundy (1994) thermometers, the predominantassociation of Mg-Hbl and plagioclase Аn40-50 crystallized at temperature of 847 ± 18 °C andpressure of about 150 MPa (~5 km depth). Some amphibole phenocrysts crystallized underhigher temperature conditions (T av. = 917º ± 23 °C, T max = 970 °C). The temperature increase
is identified not only in the cores of complexly zoned crystals but also in the rims of individual
crystals and microphenocrysts, more rarely microliths (e.g., from andesite pumice of 2013
eruption).
Heterogeneity of amphibole composition and crystallization conditions, the varies of
the crystals amount with small variations in bulk rocks and matrix glasses composition in 20012013 andesites are in good agreement with the mechanism of convective mixing. Mafic magma
replenishment should result in the formation of heated boundary layer in the lower levels of
shallow magma chamber and cause convection in its upper levels (Sparks et al., 1977). As aresult, portions of magma with different contents of crystals having a contrasting thermal
history and different amount of dissolved volatiles can reach the surface (e.g., Couch et al.
2001). Convective processes in a shallow magma chamber also may explain the Young
Shiveluch eruptive dynamics in 2001-2013. The overpressure in the magma chamber due to themafic magma input and intense emission of volatile components may cause an increase involume and frequency of eruptions.
This work was supported by a Russian Foundation for Basic Research (grant # 15-05-06640).
Referenses: Dirksen et al., 2006. J Volcanol and Geotherm Res, 155: 201-206; Couch et al., 2001.
Nature, 411:1037–1039; Gorbach, 2006. Abstracts volume of JKASP-5:133–137; Holland, Blundy,
1994. Contrib Mineral Petrol, 116: 433-447; Kiss B. et al., 2014. Contrib Mineral Petrol, 167: 986;
Leake B.E. et al., 1997 Mineral Mag, 61. (3): 295 – 321; Sato et al., 2005 J Petrol, 46 (2): 339-354;
Shevchenko A.V. et al., 2015. J Volcanol and Geotherm Res, 304: 94-107; Sparks et al., 1977. Nature,
267: 315–318; Ridolfi et al., 2010. Contrib Mineral Petrol, 160. P: 45-66.

67

LANDSLIDE AT ZНUPANOVSKY VOLCANO (KAMCHATKA) IN JULY 2015:
DISTRIBUTION OF THE DEPOSITS AND POTENTIAL PRECURSORSNatalia Gorbach1, Anastasiya Plechova2 , Dmitry Melnikov1 and Sergey Samoilenko1
1– Institute of Volcanology and Seismology FED RAS, Petropavlovsk-Kamchatsky, Russia,
n_gorbach@mail.ru
2– V.I.Vernadsky Institute of Geochemistry and Analytical Chemistry RAS, Moscow, Russia
Zhupanovsky volcano, situated 70 km north of Petropavlovsk-Kamchatsky, resumed its
activity in October 2013 (Samoilenko et al., 2014). The volcano consists of four late Pleistocene
to late Holocene cones (Fig. 1a) ranging in composition from basalts to dacites. Current activity
is associated with the youngest Priemysh cone which started to form ~3.5 14C ka BP (Bazanova
et al., 2009). Six historical explosive eruptions from Priemysh are known in 1776, 1882, 1925,
1929, 1940, and 1956-57 (Masurenkov et al., 1991). In 2014 and in the first half of 2015
episodic explosions occurred with ash columns up to 6-8 km above sea level (a.s.l)(http://www.kscnet.ru/ivs/kvert/volc.php?name=Zhupanovsky) .
On July 12, 2015 Zhupanovsky produced a strong explosive eruption, accompanied bya series of seismic events (http://www.emsd.ru/~ssl/monitoring/main.htm). The height of
explosive plumes reached 10 km a. s. l. (Senyukov et al., 2015). A smaller explosive event took
place on July 14. A few days later, on July 16, it appeared that the southern sector of Priemyshcone had collapsed covering the slopes of the volcano with a large field of landslide and lahar
deposits (Gorbach et al., 2015).
A 250-300 m-wide and ~500 m deep landslide crater was formed on the southern slopeof the Priemysh cone. The eastern wall exposes hydrothermally altered rocks andunconsolidated pyroclastic deposits while the western wall exposes fragments of lava flows,covered the slopes of the cone. The northern wall exposes a lava plug formed during previous
stages of activity (Fig. 1b).
Landslide deposits extended to southwest from the crater and covered an area of ~20
2km . Two sectors of the landslide and related deposits, western and eastern, can be clearly seenon the satellite image (Fig. 1c). The western sector is composed of debris avalanche deposits.
At a distance of ~5 km from the crater piles of blocks of different size (from a few tens of cm
to 4 m) have formed a complex topography (Fig. 1d). On July 16 the debris material in this
sector was cold and had monotonous composition corresponding to the apical part of Priemyshlava flows.
The deposits of the eastern sector have more complex structure. Closer to the crater thesurface of the deposits is smooth and composed of a layer of fine-grained gray material (fig.
1e). Such deposits are confined to depressions and to the current streams and have signs ofredeposition. In this sector the field of landslide deposits is surrounded by extensive lahar
deposits, which reach the length of ~10 km and thickness of ~5 m. On July 16 lahar deposits inplaces were soaked with water. Most likely, some of these deposits represent mixed facies ofthe debris avalanche deposits (Gliken, 1991).
At the terminal parts of the lahar deposits the mixture of blocks, ragged trunks andbranches with moistened material and the remnants of melting snow have formed a ~4 m thicksteep front. Near the front trees and bushes have been crushed, and some of them felled down.
The vegetation surrounding the landslide and lahars fronts was covered with a very thin layerof light gray ash. No signs of burning were observed on the vegetation (fig. 1f).
Landslide was not directly observed or recorded by video cameras installed near
Zhupanovsky volcano due to adverse weather conditions. However, the presence of thermal
anomaly on the satellite image TERRA ASTER (NASA, JPL) from 11:23 UTC 13 July 2015
in the southwestern sector of the volcano, coinciding with the main field of landslide deposits
68suggests that the collapse occurred in July 12 and was triggered by explosive and seismic
activity, registered on this day. The heterogeneous structure of the Priemysh cone could havecaused its edifice instability. Another factors contributing to cone instability and formation of
the water- saturated lahars may have been abundant precipitation during the month preceding
this event and presence of buried ice and snow in the saddle between the Second and Priemyshcones.

Fig. 1. Landslide at Zhupanovsky volcano: a – view of the collapsed cone and its deposits fromsouth; b – collapsed crater and lava plug in its detachment scarp; с – landslide deposits in the Westernfoot sector; d – debris avalanche deposits; e – mixed facies deposits; f – one of the lahar flows.
Referenses:
Bazanova L.I., Dirksen O.V., Kulish R.V. and Kartasheva E.V., 2009. Evolution of recent volcanism of Zhupanov
ridge (Kamchatka) // In Gordeev E.I. (eds), Proceedings of the IV All-Russian Symposium of Volcanology
and Paleovolcanology, Petropavlovsk-Kamchatsky, pp. 265-268.
Glicken H., 1991. Sedimentary architecture of large volcanic-debris avalanches. In: R.V. Fisher and G.A. Smith(eds), Sedimentation in Volcanic Settings. Sot. Econ. Paleontol. Mineral., Spec. Publ., 45: 99-106.
Gorbach N.V., Samoilenko S.B., Plechova A.A. and Melnikov D.V., 2015 // Landslide at Zhupanovsky volcano(Kamchatka) in July, 2015: first data and observation // Bulletin of Kamchatka Regional Association“Educational-scientific Center”. Earth Sciences. 3/27:5–11.
Masurenkov Yu. P., Florensky I.V., Melekestsev I.V., 1991. Zhupanovsky volcano In: Fedotov SA, Masurenkov
YP (eds) Active volcanoes of Kamchatka, vol 1. Nauka Press, Moscow, pp 84–103
Samoilenko S.B., Melnikov D.V., Chirkov S.A. et al., 2014. Activation of Zhupanovsky volcano in 2013-2014// Bulletin of Kamchatka Regional Association “Educational-scientific Center”. Earth Sciences. 1/23:21-26.
Senyukov S. L., Nuzhdina I.H., Droznina C. Ya., et al. 2015. Seismicity of Zhupanovsky volcano region in
2000-2015 // Materials of the conference "Problems of integrated geophysical monitoring of the Russian Far
East", September 27 - October 3, 2015, Petropavlovsk-Kamchatsky;
http://www.emsd.ru/conf2015lib/pdf/mon/Senyukovetc.pdf

69

GEOLOGY AND PETROLOGY OF TAISETSU VOLCANO GROUP, JAPAN;
EVOLUTION OF MAGMA AND ACTIVITY AGES.
Kosuke Ishige1, Mitsuhiro Nakagawa1, Seiko Yamasaki2, Akikazu Matsumoto2
1
Earth and Planetary System Science Department of Natural History Sciences, Graduate
School of Science, Hokkaido University, Sapporo, Hokkaido, JAPAN.
2
Geological Survey of Japan, AIST, Tsukuba, Ibaraki, JAPAN.
Taisetsu volcano group, located in central Hokkaido, is the northern part of the TaisetsuTokachi volcanic chain, which is situated at the southern end of Kuril arc. The volcanic activity
in central Hokkaido started ca. 12 Ma. Large eruptions associated with caldera formation had
repeated several times from 5 to 1 Ma. After the last caldera-forming eruption occurred 1 Ma,
the volcano group started its activity ca. 1 Ma and is composed of andesitic lava domes andstratovolcanoes. We performed a detailed geological survey combined with K-Ar dating forrepresentative samples. In addition, petrological and geochemical studies for the rocks of the
volcano group are also carried out. These reveal not only the structure and eruption history of
the volcanic group but also the temporal change of eruptive magma during 1 My.
The activity of the volcano group can be divided into two stages, Older and Younger
ones, associated with a long dormant period for ca. 0.5 million years. In the Older stage (ca. 1- 0.7 Ma), fluidal andesite lavas were effused from several eruption centers to form flat-shaped
volcanic edifices extending in N-S direction, such as Takanegahara, Chubetsu-dake andGoshiki-dake. The Younger stage began ca. 0.2 Ma. According to the location of eruption
centers and the eruption style, the stage can be divided into three sub-stages, Y1, Y2 and Y3. In
the Y1 sub-stage (ca. 0.2 Ma - ca. 34 ka), stratovolcano and several lava domes, such as
Nagayama-dake, Haku-un-dake, Ryoun-dake and Keigetsu-dake, were formed in thenorthwestern - central part. In the Y2 sub-stage, the most explosive and voluminous pyroclastic
eruption occurred ca. 34 ka to produce an eruption column and pyroclastic flows, resulting to
the formation of Ohachidaira caldera, 2 km in diameter. Pumice and ash fall deposits were
widely distributed at eastern Hokkaido. In addition, pyroclastic materials flowed down mainly
two directions, northeast and southwest. After the formation of the caldera, the activity has
continued mainly at southwestern flank of the caldera (the Y3 sub-stage) to form the Asahidake
volcano group. The Asahidake volcano is the largest edifice of the volcano group and started
its activity ca.20,000 years ago. The activity continued explosive eruption with lava effusionca. 5,000 years ago to form a stratovolcano. After that, edifice collapse occurred ca. 2,500 years
ago, resulting to the formation of a horseshoe crater, Jigokudani crater. Phreatic eruptions havecontinued since then to form many small explosion craters. The latest phreatic eruption
occurred ca. 250 years ago. Fumarole activity has continued within the crater until now.
Although the average eruption rate during the Older stage can be estimated to be >0.08 km 3
/ky, the eruption rate was 0.36 km3 /ky in the period from 0.82 Ma to 0.74 Ma. In the Younger
stage, the eruption rate of each sub-stage is as follows; >0.20 km3/ky for Y1, >1.2 km3/ky for
Y2，and >0.30 km3/ky for Y3.
Petrological features of the rocks of Taisetsu volcano group are largely different between
the Older and Younger stages. All of the rocks of the both stages are basaltic-andesite to dacite,
containing plagioclase, clinopyroxene, orthopyroxene and Ti-magnetite as phenocrysts,
associated with minor amounts of olivine and quartz phenocrysts in some rocks. In addition,70the rocks of the Older stage do not contain hornblende phenocrysts, while those of the Younger
stage usually include hornblende phenocrysts. The whole-rock SiO2 contents range from 54 to
69 wt.% for host rocks and from 52 to 59 wt.% for the inclusions. The host rocks from the Older
stage are characterized by higher contents of incompatible element such as P2O5, Zr, Y and Nb.
The rocks show higher 87Sr/86Sr and lower 144Nd/143Nd ratios, compared with those of theYounger stage. On the other hand, mafic inclusions in the rocks of the Older stage are the sameas those of the Younger stage. Although the same mafic magma has existed in the Taisetsu
volcano, the silicic magma had largely changed during the long dormancy.

71

THERMAL SUPPLY OF HYDROTHERMAL SYSTEM, A CASE STUDY OF THE
BOGDANOVICH VOLCANIC CENTER HYDROTHERMAL SYSTEM(PARAMUSHIR ISLAND, THE KURIL ISLANDS)
Olga Khubaeva, Antonina Nikolaeva
Institute of Volcanology & Seysmology, Petropavlovsk-Kamchatsky, Russia
Paramuchir Island is located at the north-east end of the Kuril-Kamchatka Arc(Fig.1). The north part of the island forms the Vernadsky Volcanic Ridge with the adjusting
North Paramushir magmatic hydrothermal convection system. [Belousov, 2002] It is closely
related to the Vernadsky Ridge magmatic structure and belongs to an andesitic type of volcanichydrothermal system [Henley, 1983].
Fig.1 Shematical structural scheme of th
Northen part of Paramushir island

1 - Prospective fouls a) more sure b) lessshure; 2- Displacement; 3 - Graben
depression; 4 – Caldera border; 5 Sourses a) thermal b) cold Gas andhydrothermal sources within Ebeko
and Bogdanovich Volcanic Centers
are surface manifestations of thissystem.
Ptichy Sourse (Т=20-45о С) withmineralization up to 0.5 g/l are
discharging at two hypsometric levels,on the east flank of Bogdanovich
Volcanic Center, at the edge of one of
the tongues of the last lava flow fromthe crater of Krasheninnikov Volcano.
The waters are slightly acidic or
nearly-neutral (pH=4-6.7) with ClSO4-Na-Ca composition. The water ofPtichy Hot Springs is of mixed origin. Although the water of these springs are much diluted we
fix elevated, compared to other springs of this group, concentrations of Na, Cl and others
chemical elements in two springs' outlets. (Na + K)/Cl dependence diagram obviously showsthat most solutions from these hot springs are on the line II (Fig. 2). Fumarole thermal sources
are shown on the line I. Probably these solutions were formed due to condensation of volcanic
gas-steam jets (HCl, HF, SO2, H2S) under subsurface conditions of hydrothermally alteredrocks. We compared the solutions from several springs (Verkhne-Yurievskie and Ebeko
Volcano), discharging within Ebeco Volcanic Center, and revealed a tendency to the shift
towards magma water (line III). Ivanov, 1961 reveals that atmospheric, gas and depth
components of fluid flow were involved during formation of Yurievskie Mineral Springs.
Ptichy Hot Springs probably were formed by the same components. Elevated concentrations ofCl, Na, SO4, B and H4SiO4 in water of Ptichy Hot Springs may evidence for hydrothermal
system located within the dipped block of Paramushir Island block system.

72

(Na+K), ppm
100000
10000

1

2

3

4

5

6

10

7

8

1

9

1000

II
I
III

100

0,1
0,1

1

10

100

Cl, ppm

1000

10000

100000

Fig 2. The Na - Cl ratio(mg / l) in hot springs in
the northern part ofParamushir Island.
1 – the source of the
Ptichya River basin; 2 –Urievsky hot springs; 3 –P2 borehole; 4 –the sourceof Ebeko Volcano; 5 – thesource of the Severyanka
River head; 6 – the sourceof the Levashova River
head; 7 – the source of the
Nasedkina River head; 8 –atmospheric precipitation;
9 – seawater.

Since no geophysical works have been carried out on the island until present, the heatsource of the Bogdanovich hydrothermal system is not completely revealed. Thus, we have to
use indirect indicators and study similar systems in other parts of the planet. For example
feathering fractures [Gorshkov, 1967] on the island provides increased permeability of the crustand the possibility of manifestation of magma generation processes.
There are many dikes and explosive craters within the Vernadsky Ridge. This may be theevidence for the basaltic heat source in the depth of the hydrothermal system. Volcanoes on
Iceland, Kamchatka, the Kuril Islands and others show that the network of basaltic dikes isoften located in long-lived volcanic centers, which are associated with contemporaryhydrothermal systems. Often basaltic dikes are the main structure, through which melt and heat
are transfered. [Belousov, 2002., Gudmundsson, 1995].
Volcanic clusters on Paramushir island [Gorshkov, 1967] with their peculiarities such as
long life, geology, morphology, petrographic and chemical composition of lava and fragmental
materials from volcanic eruptions suggest that magmatic feeding system has evolved
throughout their formation. Apparently, the dikes are the main structures that provide heat forhydrothermal systems of Paramushir Island.
References:
1. Belousov V.I., Rychagov S.N., Sugrobov V.М. Severo-Paramushirskaya…(TheNorth-Paramushir Hydrothermal-Magmatic System: Geological Structure, Conceptual
Model, Geothermal Resources// Vulkanologiya i Seismologiya, 2002. № 1. Pp. 34-50.
2. Henley R.W. and Ellis A.J. Geothermal systems ancient and modern: a geochemical
review. Earth Sci. Rev. 19, 1983.
3. Gorshkov G.S. VulkanismKurilskoy… (Volcanism of the Kuril Island Arc).М.: Nauka,
1967. Pp. 288.
4. Gudmundsson А. Infrastructure and mechanics of volcanic systems in
Iceland/Journal of Volcanology and Geothermal Research 64 (1995). Pр. l-22.
5. Ivanov, V.V., Osnovnye geologicheskye usloviya… The Basic Geological Conditionsand Geochemical Processes in the Formation of Thermal Waters in Present-Day
Volcanic Areas, Tr. Laboratorii Vulkanologii AN SSSR, 1961, issue 19, Pp. 58–68.

73

MUTNOVSKY AND GORELY VOLCANOES IN KAMCHATKA: A PERFECT
CLASSROOM FOR TEACHING VOLCANOLOGYOlga Khubaeva1, Pavel Izbekov2, Sergey Samoylenko1, and John C Eichelberger2
1
Institute of Volcanology & Seismology, Petropavlovsk-Kamchatsky, Russia
2
University of Alaska Fairbanks, Fairbanks, USA;
Unique natural objects of Kamchatka have always attracted the attention of researchers
from all over the world. Joint international field works take place in the territory of Kamchatka
for many years.
Since 2003 the International Volcanic Field School is held in Kamchatka students, PhDs
and young scientists from international research community can participate in it. The school isheld annually in the first half of August, thanks to the collaboration of the Institute ofVolcanology and Seismology (Petropavlovsk-Kamchatsky), the Vitus Bering Kamchatka State
University (Petropavlovsk-Kamchatsky) and the University of Alaska (Fairbanks, UnitedStates).
Since 2003, over 200 people from different countries of the Russian Federation, the UnitedStates, France, England, Belgium, Turkey, etc attended the school.
The scientific program of the school includes lectures by leading scientists, geologicalexcursions and oral presentations by young participants.
The main task of the school is to improve the school participants notion of modern
volcanology and associated earth sciences (geology, petrology, geophysics, seismology),
develop students' and graduate students' research capacity.
Active Mutnovsky and Gorely Volcanoes is a traditional venue of the school. On a
compact territory these volcanoes give an extremely broad insight into different types of
volcanism, one can observe the whole range of volcanic rocks (from dacite to rhyolite) anddifferent stages of volcanic process.
Mutnovsky produced more than 15 eruptions in historical time. The strongest of theseoccurred in 1848 and 1927. Its last eruption had been occurring from 1960 to 1961, and had an
explosive character. Gorely Volcano produced 8 eruptions in historical time. Its last eruption
occurred at the beginning of 1985 and was characterized by weak phreato-magmatic activity.
At the summit crater of both volcanoes intensive fumarolic activity is still prevailing.
One of the most powerful deposits of steam hydrotherms in Kamchatka was discoveredin the area of Mutnovsky Volcano.High temperature crater fumaroles (up to 800 ° C) effuse to
the surface steam and gas mixtures of typical for magmatic gases chemical composition. The
earth surface temperature of singular parts of the crater is more than 100 ° (Vakin et al., 1976).
The heat efflux from North Crater comprises more than 89400 kcal/s. Mutnovsky Volcano is
located within the North Mutnovsky volcano-tectonic zone, forming a series of large faults,
along which numerous dikes and extrusions of acid composition have been intruding since
Pliocene till presence. At the same time acidic and basic magmatism within this volcano
tectonic zone also occurs (Selyangin, 2009)
Various volcanic forms and eruptive products - lava flows, cinder cones, crater lakes wererevealed on Gorely. Thus, thanks to the variety of landscapes, forms and eruptive products,
Mutnovsky and Gorely Volcanoes are unique observation objects for young scientists,
participating in field researches (Vakin et al., 1976).
The base camp of the International Volcanic Field School is located near the observatory
at the foot of Mutnovsky Volcano and allows making circle geological routes to the crates of
Mutnovsky and Gorely Volcanoes, Mutnovsky geothermal power station, other geologicalobjects.

74

Geological excursions are accompanied by lectures and field trainings on volcanology,
mineralogy, petrography, geomorphology, seismology.
Basic geological routes on Mutnovsky and Gorely Volcanoes are led by the PhD at the
University of Alaska Fairbanks Pavel Izbekov. These research excursions allow discussing
tectonic and geodynamic setting of the Kamchatka Peninsula, catastrophic caldera-formation
volcanic eruptions, considering the role of water in geothermal and magmatic processes, as wellas many other basic and specific subjects. Lectures are co-taught by leading researchers fromthe Institute of Volcanology and Seismology, the Space Research Institute, the Moscow State
University, the University of Alaska Fairbanks (USA), and other world universities such as:
Tohoku University (Japan), Université Joseph Fourier, Grenoble, France, Paris Institute ofEarth Physics, France et al. lecture.
References:
1. Vakin Ye.A., Kirsanov I.T., Kirsanova T.P. Termal'nyye polya i goryachiye istochniki
Mutnovskogo vulkanicheskogo rayona./Gidrotermal'nyye sistemy i termal'nyye polya
Kamchatki. Vladivostok. 1976. S. 85-115. Thermal fields and hot springs in the area of
Mutnovsky Volcano. /Hydrothermal systems and thermal fields in Kamchatka.
2. Selyangin O.B. K Vulkanam Mutnovskiy i Gorelyy. Petropavlovsk-Kamchatskiy.
Kholdingovaya kompaniya «Novaya kniga». 2009. Mutnovsky and Gorely Volcanoes.
Petropavlovsk-Kamchatsky.

75

FIRE AND LIFE: MICROBIAL MEDIATION OF DEEP CARBON CYCLING
ALONG THE “RING OF FIRE”, A SUBDUCTING OCEANIC LITHOSPHERE,WESTERN ALEUTIAN ISLANDS
Heather Miller1, Jake Roush2, Taryn Lopez3, Tobias Fischer4, Matt Schrenk1,2
1
Department of Microbiology and Molecular Genetics, and 2Department of Geological
Sciences, Michigan State University, East Lansing, MI, USA; 3Geophysical Institute,
University of Alaska Fairbanks, Fairbanks, AK, USA; 4Department of Earth and Planetary
Sciences, University of New Mexico, Albuquerque, NM, USA
In collaboration with geoscientists from the Alaskan Volcano Observatory (AVO) andthe Deep Carbon Observatory (DCO), we are beginning to investigate the roles that microbialcommunities play in the cycling of deep carbon reservoirs released through volcanic activity.
As the Pacific Plate subducts along the Aleutian Trench, the mantle is subjected to intensepressures and high temperatures, resulting in the release of volatile compounds and water vapor
throughout the Aleutian island arc. We hypothesize that volcanic arc environments associatedwith subduction zones sustain unique communities of microorganisms able to utilize thesevolatiles to sustain their growth, potentially impacting the global carbon cycle.
Volcanic soil samples from four Aleutian Islands (Gareloi, Kanaga, Kiska, Little Sitkin)were collected in September 2015, and DNA from resident microbial communities was
extracted and quantified (Table 1). Using universal primer sets for the 16S rRNA gene, wewere able to confirm the presence of bacterial cells in all samples, however archaeal species
were not detected (data not presented). When we compared this general microbial diversity
and abundance data to the environmental and gas composition measurements taken at thefumarole, no obvious correlations could be made. As a result, we submitted our extracted DNA
samples for 16S rRNA sequencing (MSU Genomics Core Facility), which we hope will reveal
a pattern in microbial community composition related to the volcanic gas composition and flux.
We are also conducting shotgun metagenomic analyses of the extracted DNA to identify themetabolic potential of the volcano-hosted microbial communities to consume or assimilate
volcanic gases. This information will guide experiments aimed at the enrichment and isolationof microorganisms from the volcanic environment, which may yield information on rates andprocesses in such systems. To date, we have been able to isolate a microorganism from theGareloi volcanic soil, initially enriching for sulfur-oxidizing microbes using minimal media(pH 3.0) then plating 300mL on nutrient agar (pH 7.0), both being incubated at 40°C. Further
culturing and microbial characterization activities are underway.
The outcomes of the current study are expected to provide valuable insight into theutilization of volcanic gases by microorganisms. Resident microbial communities may be
preferentially consuming the gases being emitted to increase biomass production, or they may
be altering the gas composition currently attributed to tectonic activities. Through ongoing
work, we aim to expand this initial survey to other volcanic island arc sites along the “Ring ofFire”, with the goal of incorporating these data into current models of the global carbon cycle.

76

Table 1. Volcanic soil sample data, including geochemistry, geography, temperature, andDNA yield
Sample Collection Date
Fumarole Location

Little Sitkin

Kiska

GareloiKanga

9-Sep-15

10-Sep-15

12-Sep-15

20-Sep-15

51.96117°N,
178.49226°E

52.10575°N,
177.599194°E

51.7646°N,
178.80697°E

51.9230167°N,
177.161083°E

Fumarole Elevation (m)

166

1030

1326

1237

Fumarole Temp (°C)

98

NA

101.6

94.6

Soil Sample Location

same as fumarole

52.105833°N,
177.598861°E~10 cm fromfumarole ventfumarole ventadjacent

Elevation (m)

166

1047

1326

-

Temperature (°C)

98

7

89.1

49-94

DNA concentration (μg/g-soil)

8.9

5.05

4.7

5.65

~0.5 m away fromfumarole~4 m away fromfumarole

Background Soil Location

1 m from
fumarole

52.105833°N,
177.598861°E

Elevation (m)

166

1047

1326

-

Temperature (°C)

24

7

40.5

16.4

DNA concentration (μg/g-soil)

4.75

11.6

ND

47.75

SO2 (t/d)

ND

3.6

306

70

CO2/SO2 (molar)
Fumarole Gas
Composition(%)*

95

7

PS

PS

CH4

26.3

ND

0.41

0.03

H2

2.77

ND

51.5

0.65

Ar+O2, N2

70.9

100

48.1

99.3

Gas Fluxes

ND – none detected; PS - poorly constrained; sensor saturation; NA – not available; * - Preliminary data77THE EFFECT OF THE AD 1611SANRIKU EARTHQUAKE ON VOLCANIC
ACTIVITY IN HOKKAIDO, JAPANMitsuhiro Nakagawa1
1Earth and Planetary System Science Department of Natural History Sciences, Graduate
School of Science, Hokkaido University, Sapporo, Hokkaido, JAPAN.
After several thousand years dormancy, three active volcanoes in southwestern
Hokkaido (SW Hokkaido), Hokkaido-Komagatake, Usu and Tarumai volcanoes, started theireruptive period with large eruptions of VEI=5 during AD 1640 to 1667. It has been discussed
that these could be caused by the 1611 Sanriku earthquake (M>8). It has been recently proposedthat the source of the earthquake was distributed widely from off the eastern coast of Hokkaido
to the Sanriku area. In this research, I compile the eruptive history of active volcanoes in
Hokkaido to clarify the regional difference of the eruptive activity around 17th century. In
addition, I also compile the structure and eruptive processes of magma plumbing system ofthese three volcanoes to discuss the relationship between earthquake and volcanic eruption.
Relatively large eruptions occurred in Hokkaido from end of Plesitocene to early Holocene. In
E Hokkaido belonging to Kuril arc, two large eruptions of Me-Akandake (VEI=5) and Mashu
volcanoes (VEI=6) occurred 13 and 7 ka, respectively. Nigorikawa and Tarumai volcanoes in
SW Hokkaido belonging to NE Japan arc occurred a large eruption (VEI=5) 9 and 7 ka,
respectively. Since then, volcanoes in E Hokkaido, such as volcanoes in the Shiretoko
peninsula, Masu, Atosanupuri, Me-Akan and O-Akan volcanoes, had been active until ca. 1000
years ago. On the other hand, in SW Hokkaido, although a large eruption of VEI=5 occurred in
Tarumai volcano, smaller eruptions of VEI<3 sporadically occurred in other volcanoes. In
summary, eruptive activity in SW Hokkaido had been quite lower than that of E Hokkaido sinceca. 5000 years ago. In contrast, the eruptive activity of volcanoes in central Hokkaido belonging
to the boundary between the two arcs has been relatively low. A large eruption of VEI>4 has
not occurred in the region. In 17th century, as mentioned above, three volcanoes in SW
Hokkaido started vigorous eruptive activity and has continued their activity until now. Other
volcanoes adjacent these three volcanoes have also started their activity since then. In contrast,
although two relatively large eruptions occurred in Mashu and Me-Akandake volcanoes ca.
1ka, and Rausu volcano ca. 0.7ka, eruptive activity of volcanoes in E Hokkaido has been quite
weak since then. Although small magmatic eruption have sporadically occurred in Tokachidake
volcano in central Hokkaido, no magmatic eruptions have occurred in E Hokkaido at least since
17th century. Considering temporal change of eruptive activity of active volcanoes in Hokkaido
during Holocene, if 1611 Sanriku earthquake affected the volcanic activity, it should beemphasized that the earthquake had reduced eruptive activity in E Hokkaido, whereas it had
caused sequential eruptions in SW Hokkaido. In other word, the earthquake caused distinct
influences to southwestern and eastern part of Hokkaido, respectively.
Eruptive history, the structure of magma plumibing system and its eruption processes ofthese three volcanoes in SW Hokkaido are summarized as follows. 1) Each volcano started its
eruptive activity after a long dormancy. 2) Although whole-rock chemistry of major eruptive
magma is silicic, ranging from dacitic andesite to rhyolite, whereas their melt compositions are
similar rhyolite. 3) Each initial eruption had been caused by the injection of mafic magma into
the above silicic magma less than several years before eruption. These features suggest thatenough volume of silicic magma had been accumulated in each volcano. Thus, a large
earthquake could affect the activity of a volcano to cause mafic injection and/or activation of a
voluminous silicic magma chamber. However, there existed the interval of 30 years between
the earthquake and the initial eruption in AD 1640. This would not be consistent with the 1611
Sanriku explanation that the earthquake caused sequential large eruptions in SW Hokkaido.
78

SUMMARY OF 20-YEARS’ SURVEY OF MINERAL COMPOSITION OF THE
KARYMSKOYE CALDERA LAKE AFTER ITS 1996 HAZARDOUS ERUPTION
A.G. Nikolaeva, G.A. Karpov, A.F. Sashenkova
Institute of Volcanology and Seismology FEB RAS, Petropavlovsk-Kamchatsky, Russia,
ocean@kscnet.ru

Karymskoye Lake is located within the Akademii Nauk Caldera, which is an integral partof the Karymsky Volcanic Center (KVC) (Fig. 1). KVC is peculiar for its repeated seismictectonic, tectonic and volcanic activation [Volcanic Center…, 1974]. Early in January 1996,
two almost simultaneous events took place in KVC: eruption of the Karymsky volcano andunderwater phreatomagmatic eruption in the north part of the caldera lake (Fig. 1, 2).
Karymsky volcano outburst was preceded by the changes of seismic and tectonic environments[Fedotov, 1997], while the eruption of the lake was considered sudden and unexpected. Later,
however, we distinguished the changes of hydrochemical environment that could be interpreted
as the precursors of the lake eruption. Thus, three years before the event, the lake water showed
increased salinity. S content was also gradually elevating, as well as pH (7.20-7.45). Probably,prior to the outburst, activation of fault zones at the lake bottom caused the supply of volatiles(HCl, HF, CO, SO2, CO2, H2S, as well as H2 and He). We reported those volatiles within the
explosion funnels in the newly formed Novogodny Peninsula and in the Tokarev underwater
crater immediately after the 1996 events (see Fig. 1). Lake eruption was accompanied by the
supply of abundant heat (which melted down the ice cover of the basin) and powerful
explosions ejecting huge amounts of steam-gas mixtures and scoria-bomb materials [Fedotov,
1997]. Karpov et al. [2006] reported on enormously abundant endogen matter (about 27200t of
Cl and 203456 t of SO4) supplied to the lake and diluted in it during the underwater eruption.
Waters sampled close to the submerged eruption center showed high contents of Na, K, Mg,
Cl, F, B, H4SO4, SO4, Zn, Ni, Mn, Fe, Cu, Al, Sr. The outburst caused the formation of theTokarev underwater crater in the north part of the lake, artificial Novogodny Peninsula, breakin the northeastern rim of the caldera and powerful discharge of high-temperature thermal
waters (Piipovskiye and Plyazhnye Springs, vents in the Novogodny Peninsula, bottom
discharges we found in the Tokarev crater). This discharge source traced a narrow surface zoneof submeridional strike in the central part of the peninsula.
Color of the lake water dramatically changed from grayish-blue to turquoise-blue.
Chemical composition of the lake water also suffered drastic changes. Once fresh pond
(pH=7.2, Cl-HCO3–Na composition, salinity 130 mg/l) inhabited by salmon species
Oncorhynchus nerka (Walb.) suddenly turned acidic (pH=3.2, Cl-SO4–Ca-Na, salinity ≈ 1 g/l).
Immediately after the eruption lake water reached the temperature of 20°C being well-mixed
and lacking O2 [Karpov et al., 2006; Fazlullin et al., 2000]. Later on, using a catamaran, we
yearly sampled the lake water at two hydrochemical sites – S1 located in the center of theTokarev underwater crater, and S2 in the middle of the lake – along standard profiles of 0-1020-30-40-50-60 m (see Fig. 1). Deep hydrochemical sampling was carried out by means ofreversing water bottles.
The phenomenon observed was the first example of surveying the process of recovering
the mineral composition of the lake water after a hazardous event in it. The following significant
changes were observed in the course of the 20-year hydrochemical monitoring of the
Karymskoye Lake. By the year of 1998, lake water already showed signs of stratification bysome hydrochemical parameters (ТоС, pH, O2dissolved). In 2000 there appeared a weak trend
towards the recovery of the water chemical composition (alkalization), which became quitedistinct by 2001 [Nikolaeva et al, 2005]. Suggested was total recovery of the lake watercomposition back to the initial state (that of 1984) during the complete cycle of flushing (8-10years). But this failed to happen. In contrast, slow alkalization of the lake water occurred as79well as monotonic increase of pH (Fig. 2). Water salinity was gradually decreasing down to thedepths of 40 meters, while at deeper levels this process was even slower. In 2001 water salinity
near the Tokarev crater was reported to increase by 1/3 with depth.
Our routine surveys of the area allowed distinguishing two representative groups ofelements whose behavior could account for the hydrochemical evolution of the lake waterconsisting in the mere drop of SO4, Ca, Mg, and slow decrease of (Na+K) and particularly Cl.
The first group is postvolcanic-fumarolic, typical of acidic SO4–Cl waters occurring in volcanic
areas. It appeared in the lake water as a result of the 1996 underwater eruption. It includes Ca,
Mg and S whose sources were igneous pyroclastics (1996), wall rocks of the caldera anddissolved acidic gasses. The second group is the hydrothermal one, typical of deep thermal
waters of Cl–Na composition occurring within watered hydrothermal systems (such as Uzon,
Geyser Valley, Yellowstone). Its elements (Cl, Na+K) were supplied by the surface and bottom
discharges of thermal waters within the lake basin. Piper’s triangular diagram shows theevolution of the salinity of the Karymskoye Lake waters as monitored for 20 years (see Fig. 2).
For this period, total salinity of the lake water decreased almost three-fold. Concentrations ofbulk saline composition elements dropped as follows: Ca, Mg and SO4 > 4 times, Na and К – 3times, Cl – twice. The data obtained show that only in recent years the lake water has entered
the initial stage of intensive mixing. We consider the factors suppressing the lake water
alkalization to be insufficient mixing of the water body (seasonal), lack of storm winds, andcontribution of bottom saline solutions along the fractures from the lake bottom.
References:
1. Volcanic center: structure, dynamics, matter (Karymskaya setting). Moscow: Nedra. 1974. 260 p.
2. Karpov G.A., Nikolaeva A.G., Lupikina E.G., Bortnikova S.V., Ushakov S.V. Paculiarities of hydrochemical andgeochemical composition of the matter in the Karymskoye Lake basin during the post-hazard period (1996-2005) / Reports
on geophysical monitoring of Kamchatka. Proceedings of the scientific-technical conference, January 17-18, 2006.
Petropavlovsk-Kamchatsky. 2006. Pp. 207-217.
3. Nikolaeva A.G., Karpov G.A., Lupikina E.G., Ushakov S.V. Evolution of mineral composition of thermal spring waters
and Karymskoye Lake after the 1996 eruption // Proceedings of the Annual Conference dedicated to the Volcanologist’s Day,
March 30 – April 1, 2005, Petropavlovks-Kamchatsky. 2005. Pp. 37-47.
4. Fazlullin S.M., Ushakov S.V., Shuvalov R.A., Aoki M., Nikolaeva A.G., Lupikina E.G. Underwater eruption in the
Akademii Nauk Caldera (Kamchatka) and its effects: hydrologic, hydrochemical and hydrobiological studies // Vulkanologiya
i Seismologiya. 2000. № 4. Pp. 19-32.
5. Fedotov S.A. On the 1996 eruptions of the Akademii Nauk Caldera and Karymsky volcano in Kamchatka: researches andmechanism // Vulkanologiya i Seismologiya. 1997. № 5. Pp. 3-38.

Fig. 1. View of Karymskoye Lake. Insets: a – location of Akademii Nauk Caldera in Kamchatka; b – Karymskoye Lake prior to the hazard(1996); c – view of the newly formed Piipovskiye Springs. 1 – 1996 fissure; 2 – hydrological regime sites; 3 – thermal water discharges withtemperatures of 80-100оС (a), 40-60оС (b), 10-20оС (c); 4 – cold water discharges (2-4оС). Fig. 2. Evolution diagram of mineral compositionof the Karymskoye Lake waters (1984-2015). Inset: a – simultaneous eruptions of the two centers within KVC (1996), b – bottom discharges
within the underwater Tokarev crater, c – evolution of pH at the head of the Karymskaya River. 1 – figurative points of lake water samplingsites (by years); 2 – evolution of the lake water prior to the hazard (1984-1993…1996); 3 – evolution of the water mineral composition during
the post-hazard period (1996-2015); 4 – anticipated trend of lake water recovery back to its initial state.

80

NEW DATA ON THE EOPLEISTOCENE CATASTROPHIC CALDERA-FORMINGERUPTION IN KAMCHATKA
A.N. Rogozin, V.L. Leonov
Institute of Volcanology and Seismology, Petropavlovsk-Kamchatsky, Russia
alekseiras@yandex.ru
The work presents new data on the giant caldera. A new large caldera (15×25 km), theKarymshina caldera, has been discovered in 2006 in southern Kamchatka [1]. Three complexes
are distinguished according to consecutive stages of the caldera development: pre-calderian,caldera-forming and post-calderian. The pre-calderian stage (complex I) is assumed to have
mid-Pleiocene age (3.4 – 2.6 myr). The caldera-forming stage (complex II) has Eopleistocene
age (1.78 – 1.2 myr). The post-calderic stage (complex III) is dated to Lower and Middle
Pleistocene (0.5 – 0.8 myr). An approximate volume of material erupted during the caldera
generation was estimated to be about 825 km3, which makes a weight of 2×1015 kg. Thiseruption should therefore be considered as the largest so far known to have occurred in
Kamchatka and to be among the great eruptions worldwide [2]. A tectonic uplift(4 × 12 km × 200 m) interpreted as a resurgent dome has been reconstructed in thenorthwestern part of this caldera, bounded by straight northeast and northwest trending faults.
Also the boundary of a lake, which had existed in the caldera to the South from the resurgent
uplift, has been reconstructed.
During fieldwork in 2012-2015 a vast field of ignimbrites, traces of a large
pyroclastic flow associated with caldera Karymshina, was mapped for the first time (fig. 1).
Ignimbrites were found at a distance up to 35-40 km from the edge of the caldera. The maximum
thickness of the flow exceeds 500 m, the area of the pyroclastic flow deposits is about 298
km2, and their total volume is 84 km3. It is mainly represented by ignimbrites andcrystalloclastic tuffs related to the caldera-formation, which side with volcanic relics shaped
the border of the structure at the pre-calderic stage. At the central part of the depression the
total observed thickness of ignimbrite deposits reaches 1000 m.
It has been unambiguously established that the volcanoes of mounts Goryachaya,
Yagodnaya, Levaya Karymchina, etc., located out of the caldera, but close to the boundaries of
the caldera, are older and must be considered as evidence of a major volcanic phase thatproceeded the caldera generation. It proved by the fact that the Karymshina rocks (mostly
acid tuffs and ignimbrites) that fill the caldera in some cases lay on the lavas that compose theabove volcanoes.
New data were obtained on the setting of the rhyolite domes widely abundant in the areaof study. It was shown that they are mostly confined to the boundaries of the caldera and to theboundary of the resurgent dome situated in it. Most of the domes were emplaced much later
following caldera generation, they have ages of 0.5--0.8 Ma, and they should be regarded as aconsequence of post-caldera volcanism. The Karymshina caldera is found to have the largest
scale in high-siliceous volcanism. Total volume and area of extrusions and related lava flows
reaches 2.68 km3 and 26.44 km2, correspondingly.
The structural setting of the present-day hydrothermal systems in the area of study
has been revised. It was observed that all larger hydrothermal systems (the Bol'she-Bannaya,
Karymshina, and Verkhne-Paratunka ones) are confined to the boundaries of the
Karymshina caldera.
This work was carried out within the projects of the Far Eastern Branch, Russian
Academy of Sciences (project no. 15-I-2-031), and was supported by the Russian Science
Foundation (project no. 16-17-10035).
81

Fig. 1 a) A summary map showing theboundary of Karymshina caldera, its internal structure
and a large pyroclastic flow associated with thecaldera. Note: (1) boundary of the Karymshina
caldera and the deposits that fill it (only shown incross-section); (2) resurgent uplift; (3) rhyolite
extrusions and associated lava flows: (a) on map, (b)in cross-section; (4) areas of detected lacustrine
deposits (tuff sandstone and tuff aleurolite); (5)pyroclastic flow; (6) border pyroclastic flow (a)identified during the field work, (b) supposed; (7) precaldera volcanoes; (8) small volcanic structures
composed of basaltic lavas (a) and ore veins (b)located at edges of resurgent uplift; (9) thermal hot
springs: 1 – Bol'she-Bannaya, 2 – Karymchina, 3 –Karymshina, 4 – Verkhne-Paratunka, 5 –Apachinskie; (10) – points sampling; b) General plate
tectonic position of the Kamchatka and location of the
Karymshina caldera (black rectangle).

REFERENCES
1. Leonov V.L., Rogozin A.N. Karymshina, a giant supervolcano caldera in Kamchatka:boundaries, structure,volume of pyroclastics // J. Volcanology and Seismology. 2007. V. 1. №
5. P. 14-28.
2. Bindeman I.N., Leonov V.L., Izbekov P.E.,et al. Large-volume silicic volcanism in
Kamchatka: Ar-Ar, U-Pb ages, isotopic, and geochemical characteristics of major preHolocene caldera-forming eruptions // J. Volcanol. Geotherm. Res. 2010. V. 189. № 1-2. P. 5780.
3. Bergal-Kuvikas O.V. Geochemical studies of volcanic rocks from the northern partof Kuril-Kamchatka arc: Tectonic and structural constraints on the origin and evolution of arc
magma. Ph.D. thesis. Hokkaido University. 2015. p. 190.
82

FRAGMENTS OF CRETACEOUS SEAMOUNTS IN ACCRETIONARYSTRUCTURE OF THE KAMCHATSKY MYS PENINSULA (KAMCHATKA,
RUSSIA)
Dmitry Savelyev1, Olga Savelyeva1 , Maxim Portnyagin2, 31
Institute of Volcanology & Seismology, Petropavlovsk-Kamchatsky, Russia.
2
GEOMAR Helmholtz Centre for Ocean Research Kiel, Kiel, Germany.
3
V.I. Vernadsky Inst. of Geochemistry and Analytical Chemistry, Moscow, Russia
The geological structure of the Kamchatsky Mys peninsula is determined by its position at thejunction of major structures in the NW Pacific - the Kuril-Kamchatka island arc, Aleutian islandarc and submarine Emperor Ridge. The southern part of the peninsula is composed by theaccretionary prism of the Kronotsky paleoarc (Khotin and Shapiro, 2006). A significant part of
the accretionary complex is comprised by rocks of ophiolite association, namely mantle
peridotites, gabbro, dolerites, basalts, hyaloclastites, jaspers and limestones. Our many-year
studies showed that some Cretaceous volcanic and sedimentary rocks of the ophiolite complex
can represent fragments of an intraplate seamount, which could belong to the Emperor Ridge.
Volcanic rocks in the ophiolites are represented by basalts ranging geochemically fromtrace element depleted MORB-type to enriched OIB-type (Savelyev, 2003). Trace element andisotopic composition of a peculiar type of rocks from the ophiolite, enriched tholeiites, areparticularly close to basalts of the northernmost Emperor Seamounts, Meiji and Detroit(Portnyagin et al., 2008). Depleted tholeiites with ultradepleted melt inclusions in spinel werealso found among the volcanic rocks of the Kamchatsky Mys peninsula. The extremely depleted
compositions of the rocks and melt inclusions were interpreted to originate by high degrees ofmelting under the influence of mantle plume (Portnyagin et al., 2009). Highly depleted mantle
peridotites from the ophiolites appear to have genetic link to these ultra-depleted magmas andwere interpreted to be formed under influence of a mantle plume (Batanova et al., 2014). The
most recent finding are cumulative picrites with MgO up to 20 wt% which were found in theserpentinite melange zone fringing the ultramafic massif in its south-western part. Theirgeochemical characteristics also indicate an origin under the influence of mantle plume[Savelyev, 2014]. The groundmass of these rocks and olivine phenocrysts contain abundantsulphide globules with micro inclusions of native gold, platinum and palladium compounds[Savelyev et al., 2015]. We interpret the strong enrichment in Au and PGE as additional
evidence of plume-related origin of the rocks.
Paleoceanic sedimentary rocks exposed on the Kamchatsky Mys peninsula arerepresented by limestones and jaspers of the Albian-Cenomanian age according to theirradiolarian assemblage (Palechek et al., 2010). The rocks were formed at seamount surface at
a depth of 2-2.5 km. Two beds enriched in carbonaceous material were identified in thesedimentary sections. The formation of these beds is likely related to the oceanic anoxic events
MCE and OAE2 (Savelyev et al., 2012). During the anoxic events, the seamount surface fell inthe oxygen minimum zone, which led to the accumulation of rocks enriched in organics. Anoxic
conditions promoted the accumulation of many ore elements in carbonaceous beds, including
the platinum group elements, the source of which can be synchronous volcanic eruptions(Savelyeva et al., 2015).
Tectonic structure of the southern part of the Kamchatsky Mys peninsula corresponds
to accretionary prism. Fragments of basalt flows and carbonate-siliceous sections occur as
faulted blocks and olistoliths in siliceous tuff matrix of island-arc origin. The mantle peridotites
and gabbro compose tectonic slices (Khotin and Shapiro, 2006). This structure was formed in
the Paleogene, before the accretion of the Kronotsky paleoarc to Kamchatka in Pliocene(Lander and Shapiro, 2007). The peculiarity of this terrane is large diversity of paleoceanic
83rocks that may be related to a complex structure of the subducted oceanic plate complicated byseamounts of the Hawaiian-Emperor chain.
Lander A. V. and Shapiro M.N. The Origin of the Modern Kamchatka Subduction Zone// Volcanism and Subduction: The Kamchatka Region (J. Eichelberger, E. Gordeev, P. Izbekov,
J. Lees editors). Geophysical Monograph 172. American Geophysical Union, Washington, DC,
2007. P. 57-64.
Khotin M. Yu. and Shapiro M. N. Ophiolites of the Kamchatsky Mys Peninsula, Eastern
Kamchatka: Structure, Composition, and Geodynamic Setting // Geotectonics, 2006, Vol. 40,
No. 4. P. 297-320.
Batanova, V. G., Lyaskovskaya Z. E., Savelieva G. N., and Sobolev A. V. Peridotites
from the Kamchatsky Mys: evidence of oceanic mantle melting near a hotspot, RussianGeology and Geophysics, 2014. V. 55 (12). P. 1395-1403.
Palechek, T.N., Savel'ev, D.P., Savel'eva, O.L., 2010. Albian-CenomanianRadiolarian Assemblage from the Smaginsk Formation, the Kamchatsky Mys Peninsulaof Eastern Kamchatka // Stratigraphy and Geological Correlation, 2010. V. 18 (1). P.
63-82.
Portnyagin M., Hoernle K., Savelyev D. Ultra-depleted melts from Kamchatkan
ophiolites: Evidence for the interaction of the Hawaiian plume with an oceanic spreading centerin the Cretaceous? // Earth and Planetary Science Letters, 2009. Vol. 287. Iss. 1-2. P. 194-204.
Portnyagin M., Savelyev D., Hoernle K., Hauff F. and Garbe-Schönberg D. MidCretaceous Hawaiian tholeiites preserved in Kamchatka. Geology, 2008. Vol. 36. № 11. P. 903906.
Saveliev, D.P. Intraplate alkali basalts in the Cretaceous accretionary complex of theKamchatkan Peninsula (Eastern Kamchatka) // Volcanology and Seismology, 2003. Vol. 1. P.
14–20. (Rus).
Savelyev D.P. Plagioclase picrites in the Kamchatsky Mys Peninsula, Eastern
Kamchatka // Journal of Volcanology and Seismology, 2014. Vol. 8. Iss. 4. P. 239 -249.
Savelyev D., Botcharnikov R., Filosofova T., Portnyagin M., Danyushevsky L.
Platinum Group and Chalcophile Elements in Sulfides from Picrites of Ophiolite Complex from
Kamchatsky Mys Peninsula (Kamchatka, Russia) // Goldschmidt Abstracts, 2015. 2778.
Savelyeva O., Palesskiy S., Savelyev D. PGE in Carbonaceous Beds in the Cretaceous
Carbonate-Siliceous Section of the Kamchatsky Mys Peninsula (Russia) // Goldschmidt
Abstracts, 2015. 2779.
Savelyev D.P., Savelyeva O.L., Palechek T.N., Pokrovsky B.G. Carbon isotope curveand iridium anomaly in the Albian-Cenomanian paleoceanic deposits of the Eastern Kamchatka// Geophysical Research Abstracts, Vol. 14, EGU2012-1940, EGU General Assembly 2012.

84

GEOLOGICAL STUDY ON CALDERA-FORMING ERUPTION OF SHIKOTSU
VOLCANO, SOUTH-WESTERN HOKKAIDO : SPECIAL REFERENCE TO VENTFORMATION PROCESS AND MAGMA SYSTEM
Chiharu Tomijima1, Mitsuhiro Nakagawa1
1Earth and Planetary System Science Department of Natural History Sciences, Graduate
School of Science, Hokkaido University, Sapporo, Hokkaido, JAPAN.
Shikotsu caldera, 14 km long and 12 km wide, is located in southwestern Hokkaido,
Japan, and was formed ca. 40 ka. It has been widely recognized that the caldera-forming
eruption, the 40 ka Shikotsu eruption, started with a plinian eruption to form Spfa-1 tephra,
Shikotsu pumice fall 1, and was followed by voluminous Spfl tepra, Shikotsu pyroclastic flow
(Katsu, 1959). Thus, the sequence has been widely believed to be a typical for caldera-forming
eruption. On the other hand, Yamagata (1992) described the sequence of the 40ka Shikotsu
eruption at several proximal sites and reported the presence of large scaled lag breccia layer inthe pyroclastic flow, which suggests caldera widening during Spfl eruption. However, theeruption sequence and the precise lithofacies characteristics related to temporal change oferuptive magma have not been clearly clarified. We carry out field works and boring exploration
at several sites to reinvestigate the eruption sequence and temporal change of eruptive materials
during the caldera-forming eruption of the Shikotsu volcano.
In proximal area, tephra deposits can be divided into many geological units. Based onlithofacies characteristic of these units, the caldera-forming eruption can be divided into fivephases, Phase 1 to 5 in ascending order. Phase 1 deposit consists of the alternation of fine ashwith accretionary lapilli and pumice fall layers (Unit 1), suggesting that the eruption strated
with phreatomagmatic eruption. The tephra unit of Phase 2 is composed of three sub-units, thickpumice fall (Unit 2-1), fine ash and thin pumice fall (Unit 2-2), and pyroclastic flow (Unit 2-3)
deposits in ascending layers. These deposits suggest that large scaled plinian column wasformed and had become unstable to form pyroclastic flows (Phase 2). In Phase 3, voluminous
pyroclastic flows were generated. Phase 4 started with effusion of the lithic rich pyroclastic
flows with lag breccia , followed by pyroclastic flows. In Phase 5, the scale of eruption had
extremely decreased to produce small scaled pumice fall and pyroclastic flow deposits. Thereexists the erosional gap between layers of Phase 2 and 3, indicating possible interval. Thus, theeruption can be divided into two stages with the time gap. Although Phase 2 could be considered
as typical plinian eruption, component analysis and size distribution of units of the phasesuggest that vent widening and newly vent opening possibly occurred in the later phase. Phase
3 and 4 are climactic activity of the caldera-forming eruption. However, the occurrence of thelithic concentrated pyroclastic flow deposits strongly suggests that caldera collapse occurred
during Phase 4. Juvenile materials of the caldera-forming eruption are mainly phenocryst poor
rhyolite pumice (aphyric type pumice: A-type). However, strongly porphyritic dacitic toandesitic pumice (porphyritic type pumice: P-type) was also recognized since the activity of
Phase 4. This suggests that caldera collapse was strongly related to the activity of P-typemagma.

85

GEOCHEMISTRY OF NEOGENE-QUATERNARY MAGMATISM
SOUTHERN PART OF SREDINNY RANGE, KAMCHATKA

OF

THE

Anna Volynets 1, Maria Pevzner 2, Andrey Babansky 3
1
Institute of volcanology and seismology FEB RAS, Petropavlovsk-Kamchatsky, Russia
2
Geological Institute RAS, Moscow, Russia
3
IGEM RAS, Moscow, Russia
Sredinny Range of Kamchatka (SR), the largest volcano-tectonic structure of thepeninsula, is composed from the old (Cretaceous-Paleogene) metamorphic massif and thevolcanic belt, built in Neogene-Quaternary times. According to its structure andgeomorphology, SR can be divided to the northern and southern parts. SR N (northern part ofSR) is a narrow range stretching from Alney volcanic massif to the NE (to Tobeltsen cone oreven further) and is composed by Miocene-Quaternary volcanic rocks. SRS (southern part ofSR) has more complicated structure with two principal elements: (1) eastern flank, or main
watershed (Bystrinsky and Kozyrevsky Ridges), which is the southern continuation of SR N;
and (2) “western” flank, that has NNE strike; it begins around Sredinny metamorphic massif
and continues to the N and NE. “Western” flank is marked by the large stratovolcanoes:
Khangar, Ichinsky, Kekuknaysky, Bolshaya Ketepana, composed by Pliocene-Quaternaryrocks. Geochemistry of the SRN rocks was studied in detail by (Volynets et al., 2010). It wasdemonstrated that all rocks in SRN may be divided to two groups according their age. During
Neogene, when SR was a frontal part of the corresponding subduction system, typical islandarc rocks were erupted within SRN, with high fluid-mobile/immobile ratios (f. ex. Ba/Nb), andvery low HFSE concentrations. That has changed in Quaternary times when SR became a rearpart of the subduction system and rocks with hybrid signature started to erupt. They combine
island-arc and within-plate affinities, have lower Ba/Nb (and other fluid-mobile/immobile
element ratios) and elevated HFSE content. Average amount of the enriched mantle component
in the source of Q3-4 SRN magmas was estimated as 30% (lowest (14%) at Alney volcano andhighest (55 %) at Sedanka monogenetic zone (Volynets et al., 2010)). Geochemical
characteristics of the SRS volcanic rocks are not so well-studied. (Churikova et al., 2001)
included in their research Ichinsky volcano, which is located within SRS. They described two
types of rocks here: IAB-type and WPT-type. Rocks of both types have variably elevated fluidmobile/immobile element ratios and are enriched by HFSE to different extent, i.e. all of them
combine island-arc and within-plate signatures (from 5% enriched mantle in IAB-rocks to 35% in WPT) and may be classified as hybrid type rocks, in analogy with SRN. (Perepelov et al.,2006; Flerov et al., 2009) described Pliocene volcanic rocks, located at the northern flanks of
Ichinsky, also composed by hybrid type rocks. Therefore, rocks of Neogene age with typicalisland-arc signatures were not described in SRS. The goal of our regional work was to establish
the location and time of hybrid-type and island-arc-type volcanism within SRS. This work
includes Neogene-Quaternary rocks of the following volcanic centers in SRS: at the eastern
flanks, within the main watershed - Akhtang volcano, Anaun volcano, Kostina mt. area,
Kozyrevka mt. area; at the “western” flank - Yurtinaya mt., Khangar volcano, Ichinsky volcano,
Kekuknaysky volcano; and Uksichan volcano, which is located between these two belts. At
each volcanic massif we sampled rocks of the basement, stratovolcanoes and monogenetic
centers; for Kekuknaysky we use published data from (Koloskov et al., 2011). At the current
stage of research we used mostly elements that can be determined by XRF to include in thisstudy as many sampled sites as possible.
Large volcanic centers, located in the “western” belt – Khangar, Ichinsky, Kekuknaysky- have a long eruptive history (f. ex., K-Ar age of the initiation of volcanic activity at Khangar
caldera – 7 Ma (Pevzner et al., 2016)). They demonstrate differentiated geochemical trends(trachybasalts to pantellerites at Ichinsky; basalts and trachybasalts to trachyandesites at86

Kekuknaysky, and basalts to rhyolites at Khangar). All volcanic rocks of these centers,
including old basement rocks, have elevated Ti, Zr, Nb, low Ba/Nb, typical for Q hybrid rocksof the SRN. Difference between older and younger rocks is clearly observed only at
Kekuknaysky area, but even here all analyzed edifices have hybrid signature, with increasing
amount of enriched OIB-type component in young rocks. Plateau-effusives of Yurtinaya mt.,
located at the southernmost part of SRS (6 Ma, Volynets et al., 2016) also have hybrid signature,similar to Ichinsky basalts with ~5% of OIB-mantle in the source. Volcanic rocks, erupted
within the eastern flank of SRS, in Bystrinsky and Kozyrevsky Ridges, demonstrate quite
different compositions. All studied centers have similar geochemical characteristics: mediumK basalts to andesites (in Neogene – to rhyolites), with low to moderate Ti and HFSE
concentrations. Within the eastern flank we found typical island-arc plateau-basalts of Neogeneage (Kostina mt. area), which are practically identical to the N1-2 plateau basalts of SRN.
Quaternary rocks of the eastern flank have slightly elevated HFSE content, similar to the rocksof IAB-type of Ichinsky volcano (Churikova et al., 2001) and rocks of Alney-Chashakondzha
massif (Volynets et al., 2010) with minimal amounts of OIB-type mantle component in thesource. Rocks of Uksichan massif can’t be divided to groups according their geochemistry andage: most of the samples have hybrid signature with elevated HFSE; the concentrations arelower than in neighboring Ichinsky and Kekuknaysky volcanic massifs (“western” flank), buthigher than in Anaun volcano (eastern flank). Some of the monogenetic centers, superimposedon the old Pliocene caldera, produced low-K, -Nb, -Ti basalts with high Ba/Nb, while
underlying basement rocks have hybrid signatures. Thus, rocks of Uksichan volcano havegeochemical characteristics intermediate between typical island-arc rocks and hybrid type rocksof the “western” flank of SRS and SRN.
Conclusions. Preliminary research of the geochemical features of the N-Q volcanic
rocks of SRS shows that this part of SR has complicated geological history, with simultaneousparticipation of different types of the mantle sources in magma generation within the different,
spatially separate areas. “Western” flank of SRS is characterized by the enriched mantle in thesource from at least Miocene times. Eastern flank of SRS, from Kostina mt. to AlneyChashakondzha massif, demonstrates two age groups, different by their geochemistry, as it wasreported for SRN, but the amount of the enriched mantle component in the source of Quaternary
magmas is substantially lower in SRS than in SRN or in the “western” flank.
Financial support by RAS Presidium Program №18, IVS FEB RAS (research theme №
01201354689), GIN RAS (research theme № 0135-2014-0068), RFBR projects № 08-0500932 и 14-05-00549. The authors are grateful to V. Rodin, M. Tolstykh, B. Tugarinov, S.
Zakharov, Yu. Novikov for the help in the field, sampling and sample preparation.
Churikova T., Dorendorf F., Wörner G. (2001) Sources and fluids in the mantle wedge below Kamchatka, evidence fromacross-arc geochemical variation // Journal of Petrology. 2001. Vol. 42. № 8. P. 1567-1593.
Flerov G., Philosofova T., Puzankov M. (2009) Series of rocks of Belogolovsky volcano as a reflection of the magmagenesisof the sources at the different depths (Sredinny Range of Kamchatka) // IV Russian Symposia on volcanology andpaleo-volcanology. Petropavlovsk-Kamchatsky, 2009. V. 1. P.208-211.
Koloskov A., Flerov G., Perepelov A., et al. (2011) Stages of evolution and petrology of Kekuknaysky volcanic massif asreflection of rear zone magmatism of the Kurile-Kamchatka island arc system. Part 1. Geological position andgeochemical composition of the volcanic rocks // Volcanology and seismology. 2011. №5. P. 17-41.
Perepelov A., Chaschin A., Martynov Yu. (2006) Sredinno-Kamchatskaya zone (Pliocene-Holocene) // Geodynamic,
magmatism and metallogeny of the Eastern Russia. Vladivostok: Dalnauka. V. 1. P.382-398.
Pevzner M., Volynets A., Kostitsin Yu., et al. (2016) First data on the time of volcanism initiation in Khangar caldera(Sredinny Range, Kamchatka) // Proceedings of the annual conference on Volcanologists Day “Volcanism and related
processes”. IVS FEB RAS, Petropavlovsk-Kamchatsky, p.125-128.
Volynets A., Pevzner M., Kovalenko D., et al. (2016) First data on age, geochemistry and mineralogy of Yurtinaya mt.
plateau-effusives (Sredinny Range, Kamchatka) // Proceedings of the annual conference on Volcanologists Day“Volcanism and related processes”. IVS FEB RAS, Petropavlovsk-Kamchatsky, p.21-23.
Volynets A., Churikova T., Wörner G., et. al. (2010) Mafic Late Miocene - Quaternary volcanic rocks in the Kamchatka backarc region: implications for subduction geometry and slab history at the Pacific-Aleutian junction // Contributions tomineralogy and petrology. 2010. № 159. P. 659–687.

87

REAL-TIME EARTHQUAKE MONITORING FOR TSUNAMI WARNING
IN KAMCHATKA DURING 2011-2015
Victor N. Chebrov, Anna A. Skorkina, Danila V. Chebrov, Dmitry V. Droznin,
Dmitry A. Ototuk
Kamchatka Branch, Geophysical Survey, Russ. Ac. Sci., Petropavlovsk-Kamchatsky, Russia.
Tsunami Warning System in Kamchatka was established in PetropavlovskKamchatsky, Russia in 1956–1959 years as a direct result of the great earthquake and tsunamithat occurred in the Kuril Islands and Kamchatka on November 05, 1952 (M = 8.5). This
earthquake alerted Federal officials to the need for a facility to provide timely and effective
tsunami warnings and information for these coastal areas.
In 2006–2010 Tsunami Warning System in the Russian Far East was deeply modernized
as the response of Federal officials to the tragedy of December 26, 2004 (Sumatra earthquake).
The task of the Kamchatka Branch of Geophysical Survey, Russian Academy of Sciences, wasto develop and implement the seismological component (Chebrov et al., 2009, 2012).
In this paper we shortly describe the concept of the Tsunami Warning System (TWS)
and real-time earthquake monitoring system in Russian Far East and report on its present statusin Kamchatka.
In 2014 Kamchatka Branch of GS renewed collaboration with Local officials. And in
autumn of the same year there were 5 new strong ground motions instruments installed aroundthe city. Since then a new service appeared in real-time earthquake monitoring system, such as
mapping of instrument intensity for the (1) Petropavlovsk-Kamchatsky city and (2) Kamchatka
region. These two documents are formed automatically in real time using strong ground motion
data and supposed to be sent within 15–20 minutes since the event origin time in cases of I ≥ 1
in the city and I ≥ 3 in the region.
To date the system of seismological observations developed by the Kamchatka Branchof GS RAS includes:(1) three regional processing centers (PCs in Petropavlovsk-Kamchatsky, YuzhnoSakhalinsk and Vladivostok) equipped with satellite communication system. All of them havecomplete access to the data of all seismic stations of SSO TWS, analyze seismic data anddetermine earthquake parameters in real time in 24/7. Processing centers obtained two types of
estimations: interactive (preferred, human-controlled) and automatic (as an auxiliary alarm
signal which turns on when 7 onsets are detected);(2) seismic network, consisting of 55 strong motion instruments, 31 among them are inseismic groups around 6 principal stations, and 18 auxiliary digital stations. All stations areequipped with both accelerometers and broadband velocimeters (Tc = 120 sec). Principal
stations are located near the towns on the coast. Also data of Global Seismographic Network
and a few regional GS stations are incorporated in the data processing;(3) real time data acquisition system.
PC “Petropavlovsk-Kamchatsky” is mainly responsible for the offshore zone within thecircle area with the radius of 1000 km around PET station. The “tsunami” alert should be
released when within the area an earthquake with MS ≥ 7.0 occur.
Let cover the main results for 2011–2015.
41 regional events have KS ≥ 13.5 and/or MS ≥ 6, which are the threshold estimateswhen the Urgent Message Survey “Petropavlovsk” starts to operate as TWS. Traditionally,tsunami alerts are formed on the basis of earthquake epicenter coordinates and magnitude. The
only “tsunami” alert was sent in 2012 which turned out to be false due to depth factor. Afterthat the hypocenter criteria was checked.

88

SSO TWS is capable to release the first alert about the fact of a strong earthquake(“possible tsunami” alert) not later than 4 minutes after its origin time. For the near-fields (withradius of 200 km from PET), estimates of earthquake parameters are supposed to be sent within
7 minutes from the time of registration at the first station. In fact in 2011–2015, the average
response time to an earthquake within this area is 4 minutes 25 seconds after its origin time
(Table). The discrepancy of epicentral assessment, comparing to NEIC solutions, equals 40 km
in average.
The Urgent Message Survey “Petropavlovsk” for the same period has sent 2411
information messages including 1694 urgent messages (Table). From them there were 75
earthquakes felt in Petropavlovsk. It also should be noted that since 2015 solutions obtainedwith KS < 10 are also used to reflect the current seismicity in the region. And currently the
number of solutions produced by PC “Petropavlovsk” has increased, what is mainly the resultof saving solutions which are turned out to be after processing not strong enough to be sent asurgent messages.
To summarize, since 2015 year PC “Petropavlovsk-Kamchatsky” has been on-streamas (1) a seismological component in Tsunami Warning System, (2) Urgent Message Survey and(3) local real-time seismological information center.
Table. Distribution of solutions numbers and average response times in different zones by
years for PC “Petropavlovsk-Kamchatsky”.

2011
2012
2013
2014
2015
2015*
Total
Total*

Number ofmessages
247
347
414
329
357
1074
1694
2411

Δ≤
200 km
39
44
116
30
23
183
252
412

Average
tresponse
4 min 55 sec
4 min 09 sec
4 min 16 sec
4 min 15 sec
3 min 57 sec
5 min 47 sec
4 min 25 sec
5 min 03 sec

Δ≤1000 km
90
162
209
116
122
498
698
1075

Average
tresponse
5 min 53 sec
6 min 35 sec
4 min 54 sec
5 min 49 sec
6 min 30 sec
7 min 27 sec
5 min 51 sec
6 min 31 sec

Δ≤Δ>
2000 km 2000 km
124
123
207
140
256
158
151
178
166
191
726
348
904
790
1464
947

* The numbers reflect the quantity of both urgent and information messages. The rest results are forurgent messages only.

References
Chebrov, V.N., Gusev, A.A., Gusiakov, V.K., Mishatkin, V.N., Poplavsky, A.A. 2009. A concept ofdevelopment of a system for seismological observations with the purpose of tsunami warning in the
Far East of Russia // Seismic Instruments. V. 45. №4. P. 41-57.
Chebrov, V.N., Gusev, A.A., Droznin, D.V., Mishatkin, V.N., Sergeev, V.A., Shevchenko, Y.V.,
Chebrov, D.V. 2012. Renewed system of seismic observations for the tsunami warning in the Russian
Far East // 33rd ESC General Assembly, Russia.

89

TSUNAMI SIMULATION AND LANDSLIDE MODEL OF THE 1741 OSHIMAOSHIMA ERUPTIONKei Ioki1, Yuichiro Tanioka2, Gentaro Kawakami3, Yoshihiro Kase3, Kenji Nishina3,
Wataru Hirose3, Satoshi Ishimaru3, Hideaki Yanagisawa4
1
National Institute of Advanced Industrial Science and Technology, Japan
2
Institute of Seismology and Volcanology, Hokkaido University, Japan
3
Geological Survey of Hokkaido, Japan
4
Department of Regional Management, Faculty of Liberal Arts, Tohoku-gakuin University,
Japan
The 1741 tsunami occurred near Oshima-Oshima in Hokkaido caused great damage along
the coast of Japan Sea in Oshima and Tsugaru peninsula. Assuming that the tsunami was
generated by flowing a landslide into the sea with a sector collapse in Oshima-Oshima, thelandslide was simulated. Distribution of debris deposits, topography before the sector collapse,
and landslide volume were re-calculated from a bathymetry survey data (Satake and Kato,
2001) in the north part of Oshima-Oshima. Based on these data, the landslide was simulatedusing the integrated model of landslide and tsunami (Yanagisawa et al., 2014). As a result,distribution of computed debris deposits agrees relatively well with the distribution of debris
deposits made out from bathymetry. However, the computed debris deposits spread to northpart than debris deposits made out from bathymetry and not reach to the east and west partcompared to debris deposits made out from bathymetry in detail. The thickness of computed
debris deposits was thicker to the north part than debris deposits made out from bathymetry.
Further, model parameters and topography before the sector collapse are needed to be improved
for more realistic tsunami simulation.

90

CHARACTERIZATION OF ELECTRIC CONDUCTIVITY, PH, AND ORGANICWALLED MICROFOSSILS FOR IDENTIFYING TSUNAMI DEPOSITS: AN
EXAMPLE OF MODERN TSUNAMI AND PALEOTSUNAMI DEPOSITS IN
PACIFIC COAST LOWLANDS, HOKKAIDO AND TOHOKU, JAPAN
Yoshihiro Kase1, Keiichi Hayashi1, Gentaro Kawakami1, Kenji Nishina1, Atsushi
Urabe2, Yasuhiro Takashimizu2
1
Geological Survey of Hokkaido, Hokkaido Research Organization, Sapporo, Hokkaido,
Japan
2
Niigata University, Niigata, Japan
Introduction
For the recognition of tsunami deposits in coastal lowlands, some distinctive criteria havebeen proposed based on sedimentological analyses of modern tsunami deposits (e.g. Peters andJaffe, 2010; Goff et al., 2012). In particular, the discrimination between tsunami- and floodorigin deposits is crucial for clarifying inundation areas, occurrence ages, and recurrences(cycles) of paleotsunamis. Although analyses of sediment geochemistry and organic-walledmicrofossils are potentially crucial for the identification of tsunami deposits, they have only
been undertaken in a small number of studies (Minoura et al., 1994; Chagué-Goff et al., 2012;
GSH, 2015). Therefore, we performed geochemical analysis, namely, analysis of electric
conductivity (EC) and pH, and organic-walled microfossil analysis for previously identified
tsunami deposits to verify the effectiveness of these methods in the coastal lowlands along the
Pacific Ocean in Hokkaido and Tohoku, Japan.
Results and discussion
We collected several samples from both modern (the 2011 Tohouku-oki tsunami) andhistorical tsunami deposits (Nanayama et al., 2003; Sawai et al., 2012) along the Pacific Coastin Japan.
(1) Geochemical analysis
The supernatant solutions of the tsunami deposits, in general, showed high EC and low pH
values compared with those of peats (Fig. 1). The high EC and low pH values correspond tohigh SO42- and Ca2+ contents (Fig. 1). Some samples also showed high values of Mg2+ contents.
However, these EC and pH values are not applicable to surficial deposits, up to depths of 60–
70 cm (Fig. 1).
The high EC (high SO42- and high Ca2+) and low pH absolute values of the supernatantsolutions of the tsunami deposits are indicative of seawater inundation, although the levels of
Na+ and Cl-, the most significant components of seawater, are low (Na+; ca 44–95 ppm, Cl-; ca
9–19 ppm) and do not correspond with the EC and pH values. The SO42- may originate from
sulfides, and the low Na+ and Cl- contents probably reflect chemical leaching of soluble species.
Although the precise geochemical processes are unclear, this characterization could be a useful
method to identify tsunami deposits.
(2) Organic-walled microfossils
Some modern tsunami and paleotsunami deposits contain dinoflagellate cysts andforaminiferal linings characteristic of coastal areas, indicating shallow marine sources for the
clastics. However, other tsunami deposits do not contain organic-walled microfossils. It issuggested that differences in organic residue composition are related to variations in
geographical location and distance from the sea.
In addition, in 2011 Tohoku-oki tsunami deposits, foraminiferal linings are concentrated
only in the base of the sand beds, while dinoflagellate cysts are found both in the base of sandbeds and in the top of muddy beds (mud drapes) (Fig. 2). These results suggest density
separation of the foraminifera and dinoflagellate cysts occur through sedimentation processes.
91Hence, it is effective to examine muddy layers (mud drapes) of tsunami deposits to locate
dinoflagellate cysts.
Acknowledgement
This research was supported by the Collaborative Research Project (2015-7) of the ResearchInstitute for Natural Hazards and Disaster Recovery, Niigata University
References
Chagué-Goff et al., 2012, Sed. Geol.; Geol. Sur. Hokkaido, 2015, Special Rep. No. 42.; Goff etal., 2012, Sed. Geol.; Minoura et al., 1994, Sed. Geol.; Nanayama et al., 2003, Nature.; Petersand Jaffe, 2010, U.S. Geol. Sur. Open-File Rep.; Sawai et al., 2012, Geophy. Res. Lett.

Fig. 1. An example of stratigraphy and vertical variations in electric conductivity (EC), pH,
and Ca2+, Mg2+ and SO42- of a core sample from Yamamoto-cho, Miyagi Prefecture, Japan.
Ages of tsunami deposits are compiled from Sawai et al. (2012).

Fig. 2. Stratigraphy of the 2011 Tohoku-oki tsunami deposit and associated organic-walledmicrofossils. A and B were from muddy layers of the deposit (mud drapes) (A, B: dinocysts
gen. et sp. indet.). C–F were from basal part of the sand (C: dinocyst gen. et sp. indet. D:
Cleistosphaeridium sp., E, F: foraminiferal linings). Scale bar is 20 μm long.

92

2015-2016 ACTIVITY OF KAMCHATKAN AND NORTHERN KURILES
VOLCANOES (RUSSIA) AND DANGER TO AVIATION
Evgenii Gordeev, Olga Girina, Alexander Manevich, Dmitry Melnikov, and Anton
Nuzhdaev
Institute of Volcanology & Seismology FEB RAS, Petropavlovsk-Kamchatsky, Russia.
There are 36 active volcanoes in Kamchatka and Northern Kuriles with several of them
being continuously active. In 2015-2016, four of the Kamchatkan volcanoes (Sheveluch,
Klyuchevskoy, Karymsky, and Zhupanovsky) and two volcanoes of Northern Kuriles (Alaid
and Chikurachki) had strong and moderate explosive eruptions. Moderate gas-steam activity
was observed at Bezymianny, Kizimen, Avachinsky, Koryaksky, Gorely, Mutnovsky, and othervolcanoes.
Strong explosive eruptions are the most dangerous for aircrafts because they can send
to atmosphere up to several cubic kilometers of volcanic ash and aerosols during a few hours
or days. Ash clouds can propagate for thousands of kilometers away from a volcano remain in
the air for several days, and pose a continuous threat to aircrafts, as the melting temperature ofash particles is below operating temperatures of jet engines.
The eruptive activity of Sheveluch volcano resumed in 1980 and is continuing at present.
In 2015 strong explosive events at Shiveluch occurred on January 7, 12, and 15; February 1,
17, and 28; March 4, 8, 16, 21-22, and 26; April 7 and 12. Each time ash plumes rose up to 712 km a.s.l. and extended for more than 900 km to different directions from the volcano [3].
Ashfalls occurred in Ust’-Kamchatsk on March 16, and in Klyuchi on October 30. In the second
half of 2015 and early 2016, an intensive growth of the northern block of lava dome wasobserved, accompanied by strong and moderate hot avalanches. Aviation color code ofSheveluch was Orange during 2015-2016. Activity of the volcano was dangerous tointernational and local aviation.
Explosive-effusive eruption of Klyuchevskoy volcano lasted from January 1 to March24, 2015 [1]. Strombolian explosive volcanic activity began on January 1, 2015. On January 89 a lava flow was detected at the Apakhonchich chute on the SE flank of the volcano. Vulcanianactivity of the volcano began on January 10. Ashfalls occurred on January 11 and 28, and on
February 7 in Kozyrevsk, as well as on January 21 and 27, on February 5, 11, and 13-16 in
Klyuchi. Paroxysmal phase of the eruption occurred on February 15 when continuous series of
explosions sent ash up to 8 km a.s.l. during five hours of eruptive activity. Ash plumes drifted
for about 1000 km mainly to the east from the volcano. A thermal anomaly was observed insatellite images again on August 28 and it was registered time to time till December 31.
Aviation color code of the volcano was Yellow during January 1-11; Orange during January 11– February 15; Red on February 15; Orange during February 15 – March 25; Yellow during
March 25 April 6; Green during April 6-14; Yellow during April 14-18; Orange during April
18-26; Yellow during April 26 – May 5; Orange during May 5-13; Yellow during May 13 –July 20; Green during July 20 – August 28; Yellow during August 28 – December 31, 2015.
Next Strombolian explosive eruption began on March 3, 2016 and continues at the time of thiswriting. Volcanic explosions send bombs up to 500 m above the volcanic crater. The volcano
sometimes produces strong gas-steam plumes containing small amounts of ash. Aviation color
code of the volcano is Yellow at present. Eruptive activity of Klyuchevskoy poses a continuous
threat to international and local aviation.
Karymsky volcano has been in a state of explosive eruption since 1996. Moderate ash
explosions at Karymsky volcano were observed during 2015-2016 with ash plumes rising up
to 5 km a.s.l. and extending for more than 300 km mainly to the east from the volcano [3].

93Aviation color code of the volcano was Orange. Activity of the volcano was dangerous to local
aviation.
Explosive eruption of Zhupanovsky volcano began on June 6, 2014, and continues in
unstable regime at present time. In 2015, explosions sent ash up to 8-11 km a.s.l. on March 78 and 25, July 12, and November 30; and up to 3.5-6 km a.s.l. on other days [3]. Ash plumes
extended for about 1200 km mainly to the east from the volcano. During January 26 - February
6, February 9-15, February 23 – March 01, March 25 - April 03, April 4 to May 20, May 21 –June 8, June 16 – July 12, and July 15 – November 27 the volcano was in a state of relativequiescence. The activity culminated in explosions and flank collapses of Priemysh active coneon July 12 and 14, and November 30, 2015. Aviation color code of the volcano was Orange
from January 1 to May 16; Yellow from May 16 to June 8; Orange from June 8 to July 19;
Yellow on July 19-20; Green from July 20 to November 27; Orange from November 27 to
December 10; Yellow on December 10-17; and Green on December 17-31. In 2016, explosions
sent ash up to 8-10 km a.s.l. on January 19, 21, and 24, February 5, 7, 9, and 12, and on March
24 [2]. Ash plumes extended for about 600 km in different directions from the volcano. Aviation
color code of the volcano was Orange from January 19 till April 13, and then Yellow till present.
Activity of the volcano was dangerous to international and local aviation.
The eruption of Chikurachki volcano occurred on February 15-18, 2015 and March 2831, 2016. In 2015, ash plumes rose up to 7.5-8 km a.s.l. and extended for nearly 280 km to thewest and to the east of the volcano [3]. In 2016, ash plumes rose up to 4 km a.s.l. and extended
for about 570 km to the NE, south, and SW from the volcano. Aviation color code of the volcano
was Orange during February 16-22, Yellow on February 22-26 in 2015; Yellow on March 29– April 05 in 2016. Activity of the volcano was dangerous to local aviation.
The intensive thermal anomaly at Alaid volcano was observed in satellite images from
October 1, 2015 [3], till present. In 2016, strong gas-steam plumes containing ash rose up to 3
km a.s.l. on March 03, from March 30 till April 1 (simultaneously with eruption at Chikurachki
Volcano), and on April 9. Aviation color code of the volcano was changed to Yellow on October
1, 2015, and then to Orange on March 3, 2016. The volcano remains at Orange at present.
Activity of the volcano was dangerous to local aviation.
References
1. Girina O.A., Demyanchuk Yu.V., Mel'nikov D.V., Manevich A.G., Manevich T.M,
Nuzhdaev A.A., Muraviev Ya.D. 2015 Eruption of Klyuchevskoy Volcano and it Danger for
Aviation. In: Materials of XVIII Volcanol. Conf. “Volcanism and Processes involve with it”,
30 March – 01 April, 2015, Petropavlovsk-Kamchatsky: IVS FED RAS, 2016, pp. 16-20 (inRussian)
2. Girina O.A., Manevich A.G., Mel'nikov D.V., Manevich T.M, Nuzhdaev A.A., Lungul O.A.,
Sorokin A.A. 2016 Explosive Activity of Zhupanovsky volcano. In: Materials of XIX Volcanol.
Conf. “Volcanism and Processes involve with it”, 29-30 March, 2016, PetropavlovskKamchatsky: IVS FED RAS, 2016, pp. 24-34 (in Russian)
3. Girina O.A., Manevich A.G., Mel'nikov D.V., Nuzhdaev A.A., Demyanchuk Yu.V. 2015
Activity of Volcanoes of Kamchatka and Northern Kuriles and Danger for Aviation. In:
Materials of XIX Volcanol. Conf. “Volcanism and Processes involve with it”, 29-30 March,
2016, Petropavlovsk-Kamchatsky: IVS FED RAS, 2016, pp. 35-45 (in Russian)

94

TEMPORAL VARIATION OF THE ACROSS SIGNALS DURING A PERIOD FROMJANUARY TO AUGUST, 2015 IN SAKURAJIMA VOLCANO, JAPAN.
Hiroki Miyamachi1 , Koshun Yamaoka2 , Hiroshi Yakiwara1 , Yuta Maeda2 , Toshiki
Watanabe2 , Takahiro Kunitomo2 , Takeshi Tameguri3 , Masato Iguchi3
1
Graduate school of Science and Engineering, Kagoshima University, Kagoshima, Japan.
2
Earthquake and Volcano Research Center, Graduate School of Environmental Studies,
Nagoya University, Nagoya, Japan.
3
Disaster Prevention Research Institute, Kyoto University, Kyoto, Japan.
Quantitative monitoring of magma transport process is essentially important forunderstanding the volcanic process and prediction of volcanic eruptions. To realize thismonitoring, an active monitoring system using a vibration source called ACROSS has been
operated in Sakurajima Volcano since September 2012 (Yamaoka et al., 2014; Miyamachi etal., 2013, 2014). From our previous observational studies, we obviously found that theamplitude and travel times of the daily transfer functions (the ACROSS signal) vary temporally.
In particular Maeda et al. (2015) revealed that the amplitude of the ACROSS signals in the later
phases became small in several hours before and after explosive eruptions. In this report, weshow a long-term temporal change for the ACROSS signals observed with the remarkable
volcanic activity that occurred in Sakurajima volcano on August 15, 2015.
Our ACROSS system is composed of two vibrators: one vibrator (SKR1) with a signal
frequency range of 7.510Hz +/- 2.50Hz and the other (SKR2) with the range of 12.505Hz +/2.50Hz. The seismic signals from the ACROSS sources are routinely monitored with more than
20 permanent and 5 temporal seismic stations in and around Sakurajima volcano. The signals
recorded at the seismic stations are deconvoluted with the ACROSS source function to obtainthe transfer function between the source and the receivers. In 2015, the ACROSS system started
operation at the beginning of January 2015, but the operation was suspended on 18 August,because of the signal contamination to a monitoring seismic station for the volcano. We use thedata in 2015 to check the temporal change of transfer functions between the ACROSS source
and the seismic stations in Sakurajima island.
We calculated the daily transfer functions for each station by every 1 day stacked data
during a period of January to August 2015. Transfer functions in Sakurajima volcano indicate
large temporal variation especially in later phase part comparing to the other site such as Awaji
or Tokai area where ACROSS system is being operated. In many of the transfer function
connecting between the ACROSS source and the stations remarkable change can be seen at theend of July, 2015, though causal relationship to the volcanic event on 15 August is not clear.
We also need to make a quantitative investigation on the meteorological effect to the transfer
functions.
Reference
Yamaoka et al. (2014) Earth Planets, Space, Doi:10.1186/1880-5981-66-32.
Maeda et al. (2015) Geophys. Res. Lett., Doi: 10.1002/2015GL064351.

95

REVISITING COSEISMIC AND POSTSEISMIC DEFORMATION FROM THE 2002
DENALI, ALASKA EARTHQUAKEHugh Harper1, Jeff Freymueller1
1
Geophysical Institute, Univ. of Alaska Fairbanks. Fairbanks, AK, USA.
Given the multi-decadal temporal scale of postseismic deformation, predictions ofprevious models for postseismic deformation resulting from the 2002 Denali Fault earthquake(M 7.9) do not agree with longer-term observations. In revising the past postseismic models
with what is now over a decade of data, the first step is revisiting coseismic displacements andslip distribution of the earthquake. Advances in processing allow us to better constrain
coseismic displacement estimates, which will affect slip distribution predictions in modeling.
Previous studies have shown that two primary processes contribute to postseismic
deformation: afterslip, which decays with a short time constant; and viscoelastic relaxation,
which decays with a longer time constant.
By fitting continuous GPS time series, we have optimized postseismic relaxation time
constants, which will be used in future studies. The time series can be fit using either two
exponential decay terms (one for each postseismic process) or both a logarithmic andexponential decay term. We use a simple grid search to minimize model WRSS and findoptimal relaxation times of: 0.625 years and 8.5 years for two exponentially decaying terms;
and 0.075 years and 10.083 years, for logarithmic and exponential decay, respectively.

96

VOLCANO MONITORING(ORAL PRESENTATIONS)

97

RECENT ADVANCES IN GEOPHYSICAL MONITORING AT MOUNTCLEVELAND VOLCANO, ALASKAJohn Lyons1, Matthew Haney1, David Fee2, Cindy Werner3, Christoph Kern3, Diana
Roman4, and John Power1
1
Alaska Volcano Observatory, U.S. Geological Survey, Anchorage, Alaska, USA,2
Geophysical Institute, Alaska Volcano Observatory, University of Alaska Fairbanks
3
Cascades Volcano Observatory, U.S. Geological Survey, Vancouver, Washington, USA,
4
Department of Terrestrial Magnetism, Carnegie Institution for Science, Washington, D.C.,
USA
Mount Cleveland volcano (1730 m) is one of the most active volcanoes in the Aleutian Arc,
having had eruptive activity recorded every year since 2005. Eruptive activity is typicallycharacterized by dome growth in the central crater, followed by minor explosive activity that
often destroys the domes. In recent years, minor lava flows have extended as much as to 2-3
km down slope on the flanks of the volcano. While the majority of activity is minor, major ash
producing eruptions are a constant aviation hazard in the region and most recently occurred atMount Cleveland in 1998 and 2001.

Figure 1. Location map and web cam image from November 2014.
Mount Cleveland last erupted at 16:58 UTC on 16 April 2016. This short-lived explosive event
was the 40th explosion detected by the Alaska Volcano Observatory since 25 December 2011.
Although the volcano is frequently active, its remote location makes observations and accessdifficult and costly. Prior to 2014, Mount Cleveland was only monitored by satellite
observations or with distal seismic stations or infrasound arrays. Collaboration between the
Alaska Volcano Observatory (AVO) and the National Science Foundation (NSF) in 2014provided the opportunity to install the first local monitoring stations. Two real-time seismic
stations, an infrasound array, and a web cam now provide significantly improved monitoring
capabilities to AVO. The time to detect explosions has been greatly reduced, and frequent small
earthquakes (including a small swarm) have been observed for the first time.
Scientifically, Mount Cleveland has been minimally studied geophysically despite strong
interest in relating monitoring observations to processes at depth. Research into what makes
Cleveland tick was given a boost in 2015, when two proposals were funded to investigate thelinkages between deep and shallow earthquakes in and around the volcano and eruption
dynamics (Roman et al., NSF GeoPRISMS), and the geochemistry of gas emissions (Werner etal., Deep Carbon Observatory). A network of 12 campaign broadband seismic stations was98

deployed in August 2015 and will be recovered in July 2016. The first volcanic gas
measurements were made in August 2015, and will be repeated in July 2016. Measurements of
SO2 column concentrations were made using an upward-looking DOAS spectrometer mounted
to the helicopter skid (a FLYSPEC was also initially used). In situ gas concentrations (H2O,
CO2, SO2, H2S) were measured using a USGS Multi-GAS unit. Low molar C/S ratios derived
from these data (<3) are consistent with the presence of shallow magma in the system and theobserved growth of a new lava dome.

Figure 2. A) Thermal (IR) and B) visual observations of a new lava dome growing in thesummit crater of Mount Cleveland on 4 August 2015.

99

CONSTRAINING THE SPATIAL AND TEMPORAL VARIABILITY OF
ATMOSPHERIC CONDITIONS TO EXPLORE THE INFRASOUND DETECTION
OF VOLCANIC ERUPTIONS IN ALASKA
Alex M. Iezzi 1, 2, Hans F. Schwaiger 2, David Fee 1, Matthew Haney 2
1
Geophysical Institute, Alaska Volcano Observatory, University of Alaska Fairbanks
2
U.S. Geological Survey, Alaska Volcano Observatory, Anchorage, Alaska
Alaska’s over 50 historically active volcanoes span 2,500 kilometers, and their eruptions
pose great threats to the aviation industry and local populations. This makes both prompt
observations of explosion onsets and changes in intensity a necessity. These volcanoes are
predominantly monitored by local seismic networks in the best case, and augmented by remoteobservations including satellite imagery and infrasound arrays. Infrasound, or acoustic energy
below 20 Hz, is an especially crucial tool because it is not obstructed by frequent cloud cover(as in satellite imagery) and infrasound waves from large sources can travel hundreds tothousands of kilometers. However, infrasound station coverage is relatively sparse and strong
wind and temperature gradients in the atmosphere create multiple waveguides and shadow
zones where the propagation of infrasound is enhanced and diminished, respectively. To
accurately constrain volcanic source information and the long-range propagation of infrasoundwaves, a detailed characterization of the spatial and temporal variability of the atmosphere isvital. These properties can be constrained using a ground-to-space model similar to that of Drobet al. (2003) that is based upon numerous meteorological observations and applied to the
propagation of infrasound waves. Here we present the first results of an atmospheric condition
re-analysis system constructed by the Alaska Volcano Observatory (AVO-G2S) to accurately
characterize and model long-range infrasound propagation from volcanic eruptions.
We select a number of case studies to examine infrasound detections (or lack thereof) fromrecent eruptions of Alaskan volcanoes, including the November 2014 and March-April 2016
eruptions of Pavlof Volcano and July 2015 explosion of Cleveland Volcano. During theNovember 2014 eruption of Pavlof Volcano, it was found that discrepancies between seismic
and infrasound detection may be due to marginal wind changes, which influences theappearance and disappearance of both weak tropospheric and stratospheric waveguides. Strong
tropospheric ducting during the 21 July 2015 Cleveland eruption produced favorable
propagation conditions that likely contributed to the trigger of the alarm at a remote infrasoundarray. This was compared with weak stratospheric ducting for the 6 November 2014 explosionof similar size that did not trigger the alarm. Detailed examination of the acoustic propagation
conditions will provide additional insight into detection capability, eruption dynamics, andarray location with future work aiming to implement real-time long-range infrasoundpropagation modeling in Alaska.
Drob, Douglas P., J. M. Picone, and M. Garces. “Global morphology of infrasoundpropagation.” Journal of Geophysical Research: Atmospheres (1984-2012) 108.D21 (2003).

100

ANALYSIS OF FUMAROLE ACOUSTICS AT ASO VOLCANO, JAPAN
Kathleen McKee1, David Fee1, Akihiko Yokoo2, Robin Matoza3
1. Wilson Alaska Technical Center, Alaska Volcano Observatory, GeophysicalInstitute, University of Alaska Fairbanks, Fairbanks, AK, United States
2. Aso Volcanological Laboratory, Institute of Geothermal Sciences, Graduate School of
Science, Kyoto University, Kumamoto, Japan
3. Department of Earth Science, University of California, Santa Barbara, CA, United States
The lowermost portion of a large volcanic eruption column is dominated by momentumdriven, fluid flow processes, and is termed the volcanic jet. The perturbation of the atmospherefrom this region produces infrasound resembling jet noise. Recent work has shown that
infrasonic volcanic jet noise has similar characteristics to audible sound from jet and rocket
engines. The study of volcanic jet noise has gained much from laboratory jet-engine studies;
however, laboratory jet studies have primarily focused on pure-air jets, thereby limiting theiruse as a comparison tool to the complex (i.e., hot, multiphase) volcanic jet. Jet noise is highly
directional, which makes sampling the acoustic wavefield at a varying angle relative to the jet
access necessary to determine jet parameters. This task is achievable with a laboratory jet
engine, but presents another challenge in the volcanic case, as our observations are usually
ground based. Previous studies have noted that fumaroles, vents in volcanic environments thatissue volatiles at temperatures greater than 100°C, produce jet noise without further detailed
investigation. The goal of this work is to enhance our understanding of large-scale volcanic
jets by studying an accessible, less hazardous fumarolic jet. We aim to characterize theacoustic signature of fumaroles and evaluate if fumarolic jets scale to that of large volcanic
jets. On July 13 a new small vent opened on the southwest flank of the partially collapsed
pyroclastic cone within Naka-dake crater of Aso Volcano, Japan. The vent was several meters
in diameter and had consistent gas jetting which produced audible jet noise. We deployed a 6element acoustic array along the southwestern edge of the crater to capture the acoustic
signature of the gas jetting. The array was ~230 meters from the vent and was positioned 54
degrees from the vertical jet axis, a recording angle usually not feasible in volcanic
environments. We used Mean Cross Correlation Maxima (MCCM) to determine times ofhighly correlated signal across the array elements with a threshold of 0.8. Periods of highly
correlated waveforms are characterized by sustained, low-amplitude signal with a spectral
peak around 8-10 Hz. The signal is easily buried in wind noise and in the infrasound as well
as audible bands. We have also observed a reduction in power and decrease in correlation
between certain array elements suggesting the influence of topography along the propagation
path.

101

ERUPTION TRENDS IN THE KURILE, KAMCHATKA, AND ALASKAN ARCS
Jonathan Dehn1,2, Peter Webley1,2, Anna Worden1
1
Geophysical Institute University of Alaska Fairbanks, Fairbanks, Alaska, 99775, USA.
2
V-ADAPT Inc., 903 Koyukuk Dr. Fairbanks Alaska, 99775, USA.
Volcanic activity in the Northern Pacific Arcs have been recorded consistently over the last 40
years. Taking activity reported in eruption logs and satellite data, including thermal activity as
well as plumes, the database was divided up into quarters (Jan-Feb-Mar, Apr-May-Jun, JulAug-Sep, Oct-Nov-Dec) from January 1986 to present showing volcanic activity. This should
help account for gaps in coverage and not preferentially weight volcanoes with better
monitoring coverage. It also picks out larger eruption events and overlooks small periods ofunrest. The analysis of the 40 years of eruption data show over 400 sequences of ash producing
eruptions with some volcanic activity occurring 83% of the time. A total of 35 volcanoes haveproduced this activity, but the top 6 volcanoes (in order, Shiveluch, Bezymianny/Cleveland,
Kliuchevskoi, Karymsky, and Pavlof) are responsible for 65% of all the volcanic activity.
Shiveluch is active nearly a third of this time, and continually since 2011 (over five years at
this time). Shiveluch is also most responsible for air traffic disruption. Dome building
volcanoes are slightly more active that stratocones in this region, due to the activity at Shiveluch
and Bezymianny (77 total quarters combined). The 4 stratocones typically have very
symmetrical eruption cycles around the climax, long lead-ups leading to protracted eruptions(e.g Kliuchevskoi 2010-2011), and sudden eruptions being very brief (e.g. Pavlof, 2016). The
Kamchatka Peninsula is more active by nearly a third over the Alaska/Aleutian Arc (148 to 105
volcano quarters), yet has only 10 active volcanoes during this period compared to the 20 in
Alaska. The Northern Kurile Arc is an order of magnitude less active that the Alaska/AleutianArc.
Overall the number of quarters with plumes detected has remained stable over the time period,
suggesting that the monitoring effort is catching most if not all of the ash-producing explosions
that provide a risk to air travel. However, the precursory activity, in the form of thermal
anomalies, fluctuates over the years, and generally are greater in recent years likely representing
more attention being paid to this phenomena. There is some indication in the last three years
little thermal activity was missed and we have reached effective monitoring levels. Over 66%
of the thermal activity was followed by an ash-producing explosion, however almost one halfof the ash producing eruptions showed no thermal warning prior to the event.
Fully a third of the quarters had air travel disruption due to volcanic activity in the last 40 years.
This was rare in the early years but as monitoring and level of air traffic have increased, in thelast 5 years fully 50% of the quarters have air travel disruption. Since the global awareness of
air travel disruption from Eyjafjallajökull in 2010, even more quarters have shown air travel
disruption.

102

10

5

Kamchatka

Total

40

30

20

10

0

PlumesThermal Anomalies

30
25
20
15
10
5
0

Quarters with volcanic events

Kuriles
AlaskaKamchatka
Total

AlaskaQuarters with volcanic events

2008

2012
2014

2004

2002

2006

2010

Year

2014

2012

2010

2008

2006

2004

2002

2000

1998

1996

1994

1992

1990
1988
1986

0

2000

1986
1988
1990
1992
1994
1996
1998

KurilesYear

Volcano Quarters with Air Travel Disruption

103

INCREASING OF GAS BUBBLINGS AT WARIISHI FLOWING SPRING,CENTRAL JAPAN, PRIOR TO THE 2014 ONTAKE VOLCANO ERUPTION
Shigeki Tasaka∗ †, Masaya Matsubara†, Yasuhiro Asai∗, and Fumiaki Kimata
1
2

Tono Research Institute of Earthquake Science, ADEParth & Space Sciences, Japan.
Information and Multimedia Center, Gifu University, Gifu, Japan.

Wariishi flowing spring is located in Niigata-Kobe Tectonic Zone (NKTZ) in central
Japan, and artesian aquifer of 45 degrees are flowed from the 850 m underground with periodic
spring. Continuous monitoring of temperature and discharge volume was started at Wariishi
Spa, to make clear their change by seismic and ground deformation activities in the NKTZ in
1998 by Gifu University. An electromagnetic flowmeter is employed to measure the discharge
with sampling rates 1 to 20 Hz.
As results, hot springs of about 40
litters per minute is discharged including of
two intermittent spring with periods of about
two hours and three minutes. Co-seismic
raising discharges few to 35 litter/minutes areobserved 72 times at the big earthquakes inJapan and large earthquakes in the world in thelate 12 years since 2004 (Fig.1). Raisingdischarges are decreasing gradually with time. Fig.1 Time series of hot spring discharge at Wariishi
In contrast to discharge, the frequencies ofintermittent spring are shortening to be 20minute at the co-seismic rising discharge, andthey are coming buck to be 120-minutegradually.
On September 27, Ontake volcano, an
active volcano locates 50 km southward from
Wariishi spa, was erupted. There is no changeof discharge volume and intermittent spring
frequencies at the eruption. Discharges are
steady about 25 L/min, and it is increasing up
to 38 L/min at the M6.7 Earthquake in Fig.2 Number of bubbling between intermittent spring
Northern Nagano on November 25. The at Wariishi
frequency of intermittent spring was alsosteady about 100 to 120 minutes in the period.
Additionally, small bubbling was detected few times between main intermittent springwith a period of two hours by an electromagnetic flowmeter. Nevertheless, bubbling wasincreasing in August 2014, and it raised over 40 times in the middle of September 2014 (fig.2).
After then bubbling was decreasing, and it was few times at the end of November. It is the mostremarkable changes since 2012. As it is no definite change of discharge volume and frequency
of intermittent spring in Warisihi flowing spring, it is suggested that a bubbling system isprovided as the different process from the discharge and spring frequency. In addition, there
some changes in the strain field around Ontake volcano and Wariishi spa, and it triggered the
bubbling.

104

REMOTE SENSING ANALYSIS OF THE 2015-2016 SHEVELUCH VOLCANOACTIVITY
P. W. Webley1, O. Girina2, J. S. Shipman1
1
Geophysical Institute, University of Alaska Fairbanks, Fairbanks, Alaska, 99775, USA
2
Institute of Volcanology and Seismology, Petropavlovsk-Kamchatsky, 683006, Russia
E-mail: pwwebley@alaska.edu Phone: +1 907 474-1542 Fax: +1 907 474-7290
Sheveluch is one of the most active volcanoes of Kamchatka. Sheveluch volcanic
edifice has a complex structure, including the Late Pleistocene Old Sheveluch stratovolcano(3.283 km) complicated on its western flank with a later lava field (Baidarny ridge) and the 9km-wide caldera enclosing Holocene active Young Sheveluch (2.8km) eruptive center. In
addition, several Holocene
domes have been emplaced at
the western slopes of Old
Sheveluch.
Two large Plinian eruptionsof Sheveluch occurred in1854 and 1964 [1]. In 1980, a
new lava dome began
growing into the 1964
explosive
craterandcontinues at present. Strong
paroxysmal
explosive
eruptions connected with agrowth of the lava dome,
occurred in 1993, 2001,
2004, two in 2005, 2007, and2010 [2].
Significant explosive
activity of Sheveluch volcano
occurred in the first half of2015 with explosions sending
volcanic ash up to 7-12 km
above sea level (ASL), andash plumes extended morethan 900 km from thevolcano [3]. These events
Figure 1. Webcam snapshots of the eruption on April 12, 2015 at 03:48
occurred on January 7, 12,(A) and 03:59 UTC (B) respectively, as well as the NOAA AVHRR BTD
and 15; February 1, 17, andfrom 04:20 UTC (C) and zoomed in around the volcano (D). Also
28; March 4, 8, 16, 21-22,
included is an example of the high spatial resolution data fromand 26; and April 7 and 12,
LANDSAT 8 on April 17, 2015(Band 7, E and Band 3, F).
see Figure 1A - 1D, with
ashfall seen in high resolution
data from April 17 (Figure 1E
and 1F). Ashfall also occurred at Ust’-Kamchatsk on March 16, and Klyuchi on October 30,
2015. Strong and moderate hot avalanches, mainly from the lava dome, were observing in thesecond half of 2015.

105

In 2016, Sheveluch isstill very active as the large
lava block continues to growon the northern part of thedome over the past 11 months(since April 2015). Hot
avalanches are continuallyobserved from the westernand eastern flanks of the lava
dome. Figure 2 shows anexample of the finer spatial
resolution
data
from
LANDSAT 8 that illustrates asignificant thermal signal
from a volcanic flow ascompared to the coarser
spatial resolution advanced
very
high
resolution
radiometer (AVHRR) data at
02:15 UTC. The AVHRR
data only shows a weak signal
while the LANDSAT 8 data
Figure 2. Webcam snapshots of on March 3, 2016 activity at 00:13 (A)clearly captures the flow.
and 02:15 UTC (B) respectively, as well as the NOAA AVHRR MIR from
Combining these two datasets
02:15 UTC (C) and zoomed in around the volcano (D). Also included istogether can help us to betteran example of the high spatial resolution data from LANDSAT 8 atunderstand the ongoing
00:13 UTC (Band 8, E and RGB of Bands 765, F).
activity at Sheveluch.
We will present on
how remote sensing data has
and is being used to analyze the volcanic plumes and clouds along with the surface activity
within the summit crater and at the lava dome. We will show both the coarse spatial, hightemporal frequency data often used in real-time monitoring as well as the coarser temporal,
higher spatial resolution data to map out the thermal activity at the summit dome. We will
illustrate how by combining the datasets together along with ground observations that volcano
scientists can obtain a better understanding of the volcanic eruption and evaluate the impact tothe local region.
Acknowledgments
We would like to thank the V-ADAPT, Inc. team for access to their MIR and TIR
derived products and time series data, as well as the USGS GloVis website for access to ASTER
sensor data and the Earth Explorer site for available LANDSAT-8 data. Also we would like tothank KVERT for their monitoring and field observations and the US National Oceanic andAtmospheric Administration for access to the AVHRR data.
References
1. Fedotov, S. A. et al., 1991. Active volcanoes of Kamchatka / Ed. (1). 302 p.
2. Gordeev, E. I., and Girina, O.A., 2014. Volcanoes and their hazard to aviation, Herald of the Russian Academy of Sciences,
84, (1). 1-8. doi: 10.1134/S1019331614010079
3. Girina, O.A., Melnikov, D.V., Manevich A.G., et al, 2016. Kamchatka and North Kurile Volcano Explosive Eruptions in2015 and Danger to Aviation, Geophysical Research Abstracts, 18, doi: 10.13140/RG.2.1.5179.4001.

106

INFRASOUND AND SEISMIC OBSERVATIONS OF THE MARCH 2016 ERUPTION
OF PAVLOF VOLCANO, ALASKADavid Fee1, Matt Haney2, Robin Matoza3, Dave Schneider2, Peter Cervelli2, Alex Iezzi1
1
Alaska Volcano Observatory, Geophysical Institute, University of Alaska Fairbanks, 903
Koyukuk Dr, Fairbanks, AK 99775
2
Alaska Volcano Observatory, U.S. Geological Survey, 4230 University Drive, Anchorage,
AK 99508, USA
3
Department of Earth Science and Earth Research Institute, University of California, 1006
Webb Hall, Santa Barbara, Santa Barbara, CA 93106
On March 28, 2016, Pavlof Volcano, Alaska erupted with little to no warning. The eruption
lasted for ~40 hours and produced a sustained ash plume reaching up to 9.5 km altitude thatforced the cancellation of over 100 flights in Alaska and Canada. This eruption produced
significant seismicity, as well as infrasound that was recorded up to 1300 km away. Of
particular note is that the eruption was recorded on the recently deployed EarthScope
Transportable Array (TA), a large continental-scale network of co-located seismic and acoustic
sensors. The Pavlof eruption is the first to be recorded on the TA. Two other distant infrasoundarrays (460 and 1300 km) also recorded the eruption.
Here we present the main features of the seismic and acoustic recordings of the March 2016
Pavlof eruption, with a focus on the remote observations on the TA and infrasound arrays andthe relationship between plume height and amplitudes of seismic and acoustic data. We use a
coherence-based processing technique to detect acoustic waves on the TA and a new coherenceweighting technique to reduce noise during periods of low coherence. We also discuss thepotential to use the TA and remote infrasound arrays to detect, locate, and characterize large
volcanic eruptions in AK. Lastly, we discuss an intriguing hysteresis phenomenon between theplume height and seismic and acoustic amplitudes, where the plume heights are strongly
correlated during periods in which the eruption is intensifying and less correlated when it isdeclining. Similar hysteresis has been observed in seismicity from river discharge events.

107

THERMAL REMOTE SENSING AND ASH DISPERSION MODELING OF THE 2016
ERUPTION OF PAVLOF VOLCANO
P. Webley 1, J. Dehn1, M. Harrild1, A. Worden1, D. McAlpin1
1
Geophysical Institute, University of Alaska Fairbanks, Fairbanks, Alaska, 99775, USA
E-mail: pwwebley@alaska.edu Phone: +1 907 474-1542
Fax: +1 907 474-7290
Pavlof Volcano erupted on March 28, 2016. Alaska Volcano Observatory (AVO) firstreleased a volcanic activity notice (VAN) at 01:12 UTC on March 28 [1] while the first volcanic
ash advisory was released at 01:00 UTC [2]. We captured remote sensing data fromgeostationary and polar orbiting sensors to determine the nature and characteristics of theairborne eruptive products
during the eruption. We
demonstrate the usefulness ofthe coarser spatial resolution
data (1 km in the infrared) for
event detection and that hightemporal-resolution
brightness temperature datafrom the mid- (MIR) andthermal- (TIR) infrared timeseries can be converted into
ash cloud mass loadings using
the two band retrieval method[3].
Figure 1 shows MIR, TIR,
and brightness temperature
difference
(BTD)
data
acquired on March 28, 2016at 03:56 UTC by the
Advanced
Very
High
Resolution
Radiometer(AVHRR), together withimagery from the Advanced
Spaceborne
ThermalFigure 1. MIR (A, D), TIR (B), and BTD (C) data fromEmissionRadiometer(ASTER) sensor acquired on
AVHRR on March 28, 2016 at 03:56 UTC along with NASA
March 17 and April 11, 2016.
ASTER emissivity normalized TIR data from March 17 (E)The MIR data from 03:56
and April 11 (F), 2016.
UTC (1A and 1D) show athermal signal at the summit while the TIR (1B) and BTD data (1C) show evidence for thedispersing ash plume and cloud. The ASTER data shows weak but elevated temperatures (287K
on a background of 260K) on March 17 (1E) and April 11, 2016 (1F) that were unable to elevate
the thermal signals seen in the 1 km resolution data in either the MIR or TIR.
In addition to analysis of the remote sensing data we will also evaluate particle size
distributions (PSD) and mass eruption rates using the Puff Lagrangian Volcano Ash Transportand Dispersion (VATD) model [4]. We use a default PSD as well as coarse and fine initial
PSD’s. We will evaluate the best method to determine the mass eruption rate during an eruptive
event. Our final modeling output will include a probabilistic approach that illustrates thecapability for near real-time simulations. Figure 2 shows a model simulation from the Puff

108

VATD
model
from
March 28 – March 29,
2016. This illustrates how
the model can be used to
documenttheashlocation, mass loadings,
fallout,
andashconcentrations at specificaltitudes.
In documenting
the time series data, we
use the BTD data to
determine the direction,
length, and total masscontent of the cloud at thetime the first saturated
MIR signal is acquired.
For the Puff VATD
modeling, we illustrate
how the choice of initial
PSD and eruption rate
method are important
until more empiricalobservational data is
Figure 2. Puff VATD modeling for Pavlof Volcano, Alaska. (A)obtained.
Total mass loading (mg/m2); (B) fallout (mg/m2); (C) ash
Our work shows
particle locations by altitude (km, ASL); and (D) airborne
how the coarser spatialconcentrations (mg/m3) at 5 km ASL or FL17).
resolution data can beused to analyze the ongoing volcanic activity and to task the high resolution data for analysis
at a finer scale. Our work also illustrates the need for a probabilistic modeling approach to better
evaluate the ash mass loadings and ash concentrations.
Acknowledgements
We would like to thank the V-ADAPT, Inc. team for access to their MIR and TIR
derived products and time series data, as well as the USGS GloVis website for access to ASTER
sensor data and the Earth Explorer site for available LANDSAT-8 data.
References
1. Alaska Volcano Observatory (AVO), 2016. AVO Volcanic Activity Notice, viewed April
13, 2016.
https://www.avo.alaska.edu/activity/report.php?type=3&id=82161&mode=hans.
2. Anchorage Volcanic Ash Advisory Center (VAAC), 2016. VAA FVAK21 PAWU
280108, last viewed April 11, 2016
http://vaac.arh.noaa.gov/data/VAA/FVAK21PAWU_1603271710
3. Wen, S., and Rose, W. I., 1994. Retrieval of sizes and total masses of particles in volcanic
clouds using AVHRR bands 4 and 5. JGR: Atmospheres, 99 (D3), 5421-5431.
4. Searcy, C., Dean, K., and Stringer, W., 1998. PUFF: A high-resolution volcanic ash
tracking model. Journal of Volcanology and Geothermal Research, 80 (1), 1-16.

109

ESTIMATION OF VOLUME FLUX OF VOLCANIC ERUPTIONS WITH VERYLONG-PERIOD ACOUSTIC SIGNALS
Taishi Yamada1, Hiroshi Aoyama1, Takeshi Nishimura2, Masato Iguchi3, Muhamad
Hendrasto4
1
Graduate School of Science, Hokkaido University, Japan.
2
Graduate School of Science, Tohoku University, Japan.
3
Disaster Prevention Research Institute, Kyoto University, Japan.
4Center for Volcanology and Geological Hazard Mitigation, Indonesia.
Volume flux (or mass flux) of volcanic eruptions is a crucial parameter for the eruption
dynamics and assessment of eruption scale. There are several methods to estimate the volume
flux during volcanic eruptions, including analysis of infrasound data (e.g., Johnson et al., 2004;
Vergniolle et al., 2004). The advantage of adopting infrasound data for flux estimation is thatmost active volcanoes in the world have been monitored with infrasound network at near to
middle field and the acquisition of data can be done in real time.
In 2012–2013, we have conducted broadband seismic and infrasound observations of
Vulcanian eruptions at Lokon-Empung volcano in Indonesia. The temporal observation
network consists of 4 broadband seismometers (Trillium 40, Nanometrics, 0.025–50 Hz) andan infrasound microphone (SI 102, Hakusan, 0.05–1500 Hz). About 80 % of observed
vulcanian explosions are followed by the continuous ash emissions, which is recognized ascontinuous vibration in the seismic and infrasound waveforms. We find a clear pulse at theonset of the continuous vibration consisting of Very-Long-Period (VLP, > 10 s) signals of
infrasound and vertical velocity waveforms. The apparent propagation velocity of the VLP
pulse at each station can be explained by the sound velocity from the vent. Moreover, thegeneration of the VLP pulse approximately coincides with the appearance of ash plume fromthe vent. Hence, it is regarded that the VLP pulse is induced by pressure wave accompanying
the formation of the ash plume. Such the VLP signals accompanying eruptions also can be seenin microbarograms of ash emission eruptions at 3 Japanese volcanoes (Shinmoedake, Aso,
Kuchinoerabu) in 2011-2016. National research Institute for Earth science and Disasterprevention (NIED) has operated several barometers (AP 270, Koshin; PTB 100, Vaisala) at 27 km from the vent at those volcanoes. Since the microbarogram data is recorded at 1 Hz, the
VLP signals are properly recorded microbarograms accompanying eruptions.
We estimate the volume flux during those eruptions with the VLP signals on infrasoundrecords and microbarograms. Largely there are two methods to describe the source ofinfrasound signals accompanying eruptions; monopole and dipole approximations (Johnson etal., 2014; Vergniolle et al., 2004). The volume flux estimated by the monopole approximationand observed plume height show well agreement with the empirical relationship between thesetwo parameters (e.g., Sparks et al., 1997). Our study suggests that the volume flux can be
estimated with infrasound and microbarogram data in quasi real time due to its simplicity of
waveform processing.

110

NUMERICAL MODEL OF TEMPORAL CHANGES IN MAGNETIC TOTAL FIELDAND GROUND DEFORMATION DUE TO HYDROTHERMAL SYSTEM IN
VOLCANOES (1). - A CASE STUDY ON TOKACHI-DAKE VOLCANO, JAPANRyo Tanaka1, Takeshi Hashimoto1, Tsuneo Ishido2, Nobuo Matsushima2
12

Hokkaido University, Japan
National Institute of Advanced Industrial Science and Technology (AIST), Japan

Localized temporal changes in the magnetic total field and ground deformation are often
observed at volcanoes that have hydrothermal system within. At Tokcahi-dake volcano, one ofsuch volcanoes in central Hokkaido, Japan, continuous magnetic field changes accompanying
ground inflation at a shallow depth have been observed. At this volcano, small phreatic
explosions took place commonly among major magmatic/phreatomagmatic eruptions inrecorded history (JMA, 2013). Repeated magnetic total field surveys since 2008 revealed
demagnetization beneath 62-2 crater between 2008 and 2009 (Hashimoto et al., 2010). Besides,
the baseline changes by GPS suggested a localized inflation beneath the crater after 2007 (JMA,2015). Assuming the thermomagnetic effect, Hashimoto et al. (2010) proposed a possible
mechanism for such changes. They suspected that steam ascending along the conduit
experienced phase change at a shallow depth, releasing latent heat and flowing back as liquid
to form a hydrothermal reservoir. They also suggested that increase in heat supply from depth
is not essential for the demagnetization in case that heat discharge rate from the crater has been
reduced for some reasons. In this study, we verify such a conceptual model by using a numericalsimulation of hydrothermal system.
In general, phreatic explosions need substantial amount of water, cap-rock structure that
confines pressure, heat supply and increase in pressure for a hydrothermal reservoir to flush
through an abrupt phase change. However, it remains an open question whether such structure
and processes bring about observable magnetic changes and/or ground deformation preceding
to a phreatic eruption. We addressed the following working hypothesis to model Tokachi-dake
as a case study. (1) There is a cap-rock structure with a narrow crack below 62-2 crater. (2)Gases through the crack are discharged as plumes from the crater. (3) Decreasing permeabilityof the crack causes increase in temperature and pressure around the cap-rock structure. We tried
to examine the hypothesis using the numerical code “STAR” with the equation-of-state“HOTH2O” (Pritchett, 1995). It enabled us to calculate the heat and mass flow rate of H2O(gas, liquid and two-phase) in porous media. The calculation region was set as approximately
the cross-section passing the summit of Tokachi-dake, 62-2 crater and hot spring located on
halfway up the mountain. Firstly, we estimated the background permeability of rockconstituting the volcano, which gives a plausible water table. As boundary conditions, constanttemperature and pressure conditions were applied to the ground surface and downstream
vertical boundary, thermally-insulating and impermeable conditions were applied to the bottom
and upstream vertical boundaries. A constant rate of precipitation was injected from the groundsurface. A constant heat flow was supplied from the bottom. Subsequently, we reproduced thefumarolic discharge from the crater and the hot spring located in the middle of the slope by
providing thermal water from the bottom just beneath the crater. We also introduced a highpermeability column as a vertical conduit connected from the volcanic input at the bottom tothe crater, as well as a horizontal channel connected to the hot spring. In addition, the low
permeability cap-rock with a narrow crack was introduced below the crater. Finally, wechanged the crack permeability to observe changes in temperature and pressure of the system.
We confirmed that the decrease of the crack permeability caused the increase in temperatureand pressure around the cap-rock structure. These results suggested that the working hypothesis
111was at least self-consistent. In the next step, we will quantitatively investigate the system's
responses by comparing the changes in temperature and pressure beneath the crater from thenumerical simulation to the observed temporal change in the magnetic total field and grounddeformation.

112

EVALUATING THE INFLUENCE OF DATA GAPS IN THE ANALYSIS OFPOSITION TIME-SERIES DERIVED FROM GPS CONTINUOUS STATIONS
Rui Fernandes1, Machiel Bos1, Rafael Couto1, J. Freymueller2, Maksim Tretyakov3
1
SEGAL (UBI/IDL), Covilhã, Portugal.
2
University of Alaska, Fairbanks, Alaska, USA.
3
NEFU, Yakutsk, Russia.
Time-series derived from CORS (Continuous Operating Reference Stations) GPS
stations have significant advantages when compared with campaign-type solutions. In addition
to reduce the potential error sources (e.g., offsets due to reoccupation accuracy and/or different
receivers and antenna), they permit to extract more information concerning the different
geophysical signals, like the secular motions, periodical (annual or semi-annual) signals, co-,post-seismic or volcanic deformation.
However, particularly at very remote locations, it is often difficult to ensure thecontinuous operation of the stations due to logistic and/or financial issues: lack ofcommunication that prevent the early detection of problems; transportation, extreme weather
events; equipment failures, etc.
This was the case of the Bezymianny GPS network, which has been installed in 2006.
The network consisted of 10 permanent sites distributed around the volcano edifice. However,
due to the extreme difficult conditions, most of the time-series contain large periods with noobservations (mainly caused by power failures).
In this work, we investigate the influence of such data gaps on the estimation of thegeophysical signals, namely secular motions and periodical signals. We use a network of global
stations to determine threshold values relative to the percentage of data gaps (in terms of lengthand number) on the time-series that start to change significantly the estimated parameters.
Finally, we also apply these values to the time-series obtained for the Bezymianny GPS
network in order to quantify how much the existing data gaps have influenced the estimatedsolutions for the data acquired between 2006 and 2010.

113

TSUNAMI(ORAL PRESENTATIONS)

114

HYPOTHETICAL TECTONIC TSUNAMI SOURCES ALONG THE EASTERNALEUTIAN ISLAND ARC AND ALASKA PENINSULA FOR INUNDATION
MAPPING AND HAZARD ASSESSMENT.
Dmitry Nicolsky1, Elena Suleimani1, Jeffrey Freymueller1, and Richard Koehler2
12Geophysical Institute, University of Alaska Fairbanks, Fairbanks, AK 99775, USA
University of Nevada, Reno, Nevada, USA

The Alaska Earthquake Center conducts tsunami inundation mapping for coastal communities
along the Alaska Peninsula and eastern Aleutians. Tsunami threatened communities are
distributed along several segments of the Aleutian Megathrust, each segment is characterized
by a unique seismic history and tsunami generation potential. A critical component in thetsunami modeling is accurate identification and characterization of potential tsunami sources.
Our study area extends from the eastern half of the 1957 rupture zone to Kodiak Island, covering
the 1946 and 1938 rupture areas, the Shumagin gap, and the western part of the 1964 rupturearea. We employ data on the slip deficit along the Aleutian Megathrust, based on GPS campaign
surveys, analysis of the seismic reflection data across the arc, the Slab 1.0 interface surface,empirical magnitude-slip relationships, and the numerical code that distributes slip among the
subfault elements. We define hypothetical asperities along the megathrust and in down-dip
direction. We then calculate coseismic deformations and perform a set of sensitivity model runs
to identify coseismic deformation patterns resulting in highest runup at a given community.
Because of the extra fine discretization of the interface, we prescribe variable slip patterns, bothalong strike and in the down-dip directions. We show that the near-field tsunami runup in target
communities is sensitive to variability of slip along the rupture area.
We perform simulations for each source scenario using AEC’s numerical model of tsunami
propagation and runup, which is validated through a set of analytical benchmarks and tested
against laboratory and field data. Results of numerical modeling combined with historicalobservations are compiled on inundation maps and used for site-specific tsunami hazard
assessment by local emergency planners.

115

REGIONAL TSUNAMI HAZARD MAP FOR COMMUNITIES ON ALEUTIANISLANDS AND ALASKA PENINSULA
Elena Suleimani1, Dmitry Nicolsky1, and Richard Koehler3
1Geophysical Institute, University of Alaska Fairbanks, Fairbanks, Alaska, USA.
2
University of Nevada, Reno, Nevada, USA.
The Alaska Earthquake Center conducts tsunami inundation mapping for coastal
communities in Alaska by assessing potential tsunami sources and modeling the tsunami wave
dynamics. Over the past two decades, high-resolution tsunami inundation maps were developed
for more than 20 communities. In these studies, we performed numerical modeling of tsunami
waves for each community using high-resolution digital elevation models (DEMs) of combined
bathymetry and topography, which have been verified with local real-time kinematic GPS
surveys. The potential inundation according to various tsunamis was simulated with the best
available high-resolution data with a typical spatial resolution of 15 m. We also performed
source sensitivity studies to determine a possible slip distribution for the worst-case credible
tsunami events. In addition, multiple constraints such as regional seismicity, tectonic processes,
and geodetic and paleotsunami data were taken into account.
In the regional tsunami hazard assessment we use a different approach, because thecurrently available DEMs of many Aleutian communities lack high-resolution bathymetry andtopography data and do not satisfy the requirements for high-resolution numerical modeling of
the tsunami inundation. We follow the National Tsunami Hazard Mitigation Program(NTHMP) guidelines for determining tsunami hazard zones in areas that have either low risk
due to small population size and minimal infrastructure vulnerability, or are not scheduled toreceive high-resolution tsunami inundation maps in the near future.
To develop a regional tsunami hazard map, we consider three potential ruptures with auniform slip distribution along the strike, which are positioned on the Alaska–Aleutian
subduction interface. The three sources differ in the down-dip slip distribution pattern such thatthe depth range at which the maximum slip occurs varies from the shallow region near to thetrench to the deeper parts of the plate interface. All ruptures have the same extent, which isdetermined by the location of communities and constrained by the seismic moment. For each
community, we simulate a limited number of significant potential tsunamis and develop an
approximation to a tsunami hazard map, which is needed to support informed decision making
in the event of a tsunami, and can also help with advance development of tsunami evacuation
strategies.

116

AUTHORS INDEX
Akita, 18
Aldridge, 28
Alvizuri, 57
Aoyama, 110
Asai, 104
Babansky, 86
Baranov, 40
Bartlett III, 50
Bergal-Kuvikas, 52
Bindeman, 52
Bos, 113
Braun, 61
Braunmiller, 17
Bruner, 50
Bykov, 65
Cameron, 54
Cervelli, 107
Chebrov, 19, 88
Chomiak, 47
Connor, 58
Coombs, 48
Couto, 113
Crass, 54
Deacon, 50
Dehn, 102, 108
Droznin, 19, 88
Droznina, 19
Eichelberger, 74
Farrell, 20
Fedotov, 59
Fee, 28, 98, 100, 101, 107
Fernandes, 113
Fischer, 45, 76
Frank, 19
Freymueller, 30, 32, 37,
96, 113
Gardine, 30
George, 58

Gerasimenko, 25, 65
Gilchrist, 35
Girina, 93, 105
Gorbach, 66, 68
Gordeev, 19, 64, 93
Gusev, 23
Haney, 21, 26, 28, 98,
100, 107
Harper, 96Harrild, 108
Hashimoto, 111
Hatfield, 42, 50
Hayashi, 91
Hendrasto, 110
Hirose, 90
Hoernle, 40
Holtkamp, 17, 22, 30
Honda, 63
Ichiyanagi, 63
Iezzi, 47, 100, 107
Iguchi, 95, 110
Ioki, 90Ishido, 111
Ishige, 70
Ishimaru, 90
Izbekov, 42, 51, 64, 74
Jellinek, 35
Jicha, 48
Karpov, 79
Kase, 90, 91
Kaufman, 42
Kawakami, 90, 91
Kelly, 26
Kern, 26, 98
Khubaeva, 72, 74
Kimata, 104
KIRBY, 13
Kiryukhin, 59

Kliapitskiy, 52
Koehler, 115, 116
Kozyreva, 61
Krylovich, 42
Kunitomo, 95
Larsen, 55
Latchman, 58
Leonov, 52, 81
Li, 37
Lopez, 45, 76
Lough, 49
Lyons, 26, 42, 98
MacInnes, 42
Maeda, 62, 95
Manevich, 93
Matoza, 28, 101, 107
Matsubara, 104
Matsumoto, 70
Matsushima, 111
McAlpin, 108
McKee, 101
McNutt, 17, 20, 29, 58
Melnikov, 68, 93
Meng, 25
Merz, 61
Meyer, 61Miller, 76
Minato, 18
Miyagi, 63
Miyamachi, 95
Mochizuki, 62
Mulliken, 54
Nakagawa, 70, 78, 85
Nakahigashi, 62
Neal, 42
Nechaev, 65
Neill, 43
Nicolaysen, 42, 50
117

Nicolsky, 115, 116
Nikolaeva, 72, 79
Nishimura, 110
Nishina, 90, 91
Nuzhdaev, 93
Nye, 43
Obara, 62Ohzono, 18, 25, 65
Okazaki, 18, 63
Okuno, 42
Ototuk, 88
Patrick, 26
Persico, 42Pevzner, 86
Philosofova, 66
Plank, 49
Plechova, 68
Portnyagin, 40, 66, 83
Power, 42, 98
Proussevitch, 51
Prytkov, 65
Pupatenko, 65
Rasmussen, 49
Rizzo, 45
Rogozin, 52, 81
Roman, 49, 98
Roush, 76
Ruppert, 30, 37, 61
Sahagian, 51
Samoilenko, 68
Samoylenko, 74
Sashenkova, 79

Savelyev, 83
Savelyeva, 83
Savinetsky, 42
Schaefer, 54, 55
Schneider, 107
Scholl, 13
Schrenk, 76
Schwaiger, 100
Scott, 42
Serovetnikov, 64, 65
Shapiro, 19
Sheffer, 50
Shestakov, 25, 65
Shinohara, 62
Shiobara, 62
Shipman, 105
Silwal, 60
Skorkina, 23, 88
Smith, 29
Sorokin, 65
Stelling, 49
Suleimani, 115, 116
Suzuki, 18
Sysoev, 65
Takagi, 63
Takahashi, 18, 25, 63, 64,
65
Takashimizu, 91
Tameguri, 95
Tamura, 63
Tanaka, 111
Tanioka, 90

Tape, 30, 57, 60
Tasaka, 104
Thompson, 17, 29, 47
Titkov, 65
Tomijima, 85
Tretyakov, 113
Trusdell, 26
Tsai, 21
Uchida, 33
Urabe, 91
Vallance, 55
Vasilenko, 65
Volynets, 86
Wallace, 54
Wang, 37
Ward, 21
Watanabe, 95
Webley, 102, 105, 108
Werner, 26, 40, 98
West, 30, 42, 50, 61
Worden, 102, 108
Yakiwara, 95
Yamada, 62, 110
Yamaguchi, 63
Yamaoka, 95
Yamasaki, 70
Yamashita, 62
Yanagisawa, 90
Yogodzinski, 40
Yokoo, 101
Yokoyama, 39

118