Bull. Volcanol. Soc. Japan
Vol. /- (,**2) No. /, pp. +/+ῌ+/1

Letter

The Tephra Layers Distributed around the Eastern Foot of the Zao Volcano
ῌAges and Volumes of the Za-To + to . Tephrasῌ
Kotaro MIURA῍, Masao BAN῍῍ and Hiroshi YAGI῍῍῍(Received, February ,3, ,**2 ; Accepted, October 3, ,**2)
Ages of four scoriaceous volcanic sand layers (Za-To + to .) distributed around the eastern foot of the Zao
volcano are determined to be ca. --ῌ-,, -*.1, ,1.+, and +,.3 cal kyr BP, respectively, based on four newly obtained
radiocarbon dates and loess chronometry. Besides, we detect To-H (To-HP) glasses from the loess below the
Za-To . tephra. The estimated age of the loess horizon is consistent with the previously reported one for To-H
(To-HP). Volumes of Za-To + to . tephras are estimated to be ca. -῍+*ῌ,, -῍+*ῌ+, +῍+*ῌ+ and +῍+*ῌ+ DRE
km-, respectively, and the averaged discharge rate from Za-To + to . is calculated to be ca. *.*,ῌ*.*- km-/ky.
Key words : Zao volcano, tephra layers, radiocarbon dating, volcanic glass, discharge rate+. Introduction
The Zao volcano is a stratovolcano which is locatedin the central part of the volcanic front of the northeast
Japan arc (Fig. +). This volcano started its activity at
about + Ma (Takaoka, et al., +323), and has continued
to the present day. Geologic and petrologic studies of
the whole of the eruptive products were performed byvarious authors (e.g. Chiba, +30+ ; Oba and Konda,+323 ; Sakayori, +33,), and according to these studies,
the newest stage of the Zao volcano began at ca. -* ka,
and numerous small to medium sized eruptions havecontinued for the past -*-ky. At about -* ka, the horseshoe-shaped Umanose caldera (+.1 km in diameter),which is located in the central part of the Zao, wasformed by explosive eruptions (Sakayori, +33,). The
newest cone Goshikidake is situated in the inner part of
the Umanose caldera and the newest crater lake Okama
is located in the western part of the Goshikidake.
Tephro-stratigraphy is very useful to establish thedetailed eruptive history of volcanoes (e.g. Thorarinsson,+32+). In the case of the Zao newest stage, the tephrostratigraphic studies were performed by various authors(e.g., Imura, +330, +333 ; Itagaki et al., +32+ ; Saigusa
and Shoji, +32.). Imura (+333) recognized ten volcanic
sand layers (Za-To + to +*). Za-To + to . tephras aremostly distributed around the eastern foot of the Zao
volcano, while Za-To / to +* are mainly near the summit

area. Imura (+333) also estimated that the ages of
Za-To + to . tephras are older than ca. ,* ka, based ona radiocarbon age (Itagaki et al., +32+), and the estimated AT (Aira-Tn tephra) horizon. AT is a widespread tephra ejected from the Aira caldera about ,3 cal
kyr BP (Okuno, ,**,), widely distributed in Japan. In
the Zao, AT volcanic glasses which is the bubble wall
type (Machida and Arai, ,**-) are found in the upper
part of the loess below the Za-To . tephra (Imura,+330). In this study, we determined the ages of Za-To+ to . tephras layers based on newly obtained fourradiocarbon dates, coupled with the loess chronometry(Hayakawa, +33/) and tephrochronology. Using thisnew age data and the magma discharge volume estimated from the isopach maps, we have calculated themagma discharge rates during the Za-To + to . activities.

῎Division of Interactive Symbiosphere Sciences, Grad-῎῎῎Department of Information, Environmental and Fooduate School of Science and Engineering, Yamagata
University, +ῌ.ῌ+,, Kojirakawa-machi, Yamagata, 33*ῌ
2/0*, Japan.
῎῎Department of Earth and Environmental Sciences, Faculty of Science, Yamagata University, +ῌ.ῌ+,, Kojirakawa-machi, Yamagata, 33*ῌ2/0*, Japan.

Sciences, Faculty of Education, Art and Science, Yamagata University, +ῌ.ῌ+,, Kojirakawa-machi, Yamagata,33*ῌ2/0*, Japan.

,. Stratigraphic description of the Za-To + to . tephra
layersZa-To + to . tephra layers consist of scoriaceous
volcanic sand, and are well sorted and laminated. In
an outcrop at Haraobi (Loc. 1 ; Fig. +), all of the Za-To+ to . tehpra layers can be observed and they areintercalated in the brown colored loess (partly reddishdark brown colored paleosol), observed at the easternfoot of Zao.

Corresponding author : Masao Ban
e-mail : ban@sci.kj.yamagata-u.ac.jp

152

Kotaro MIURA, Masao BAN and Hiroshi YAGI

Fig. +. Maps showing the location of the Zao volcano (a), location of the outcrop (b), correlative stratigraphic columns
for representative sections (c) and isopach maps of Za-To + to . tephra layers (d). Topographic contour lines in(b) are at +** m intervals. P and L-+ to 0 in (c) indicate the horizons of the paleosol samples and the analyzed
volcanic glasses, respectively (see text for detail). The estimated sedimentation rates are also shown in the columnsof Loc. 0 and 1 (see text for detail). Numbers in (d) indicate the measured thickness of the layers in cm.

The Tephra Layers Distributed around the Eastern Foot of the Zao Volcano
Table +.

153

Radiocarbon data and calibration ages.

*, Samples dated at the Paleo Labo Tokai branch.
**, Samples dated at the Tono Geoscience Center.
a) Calibration age based on the calibration program CALIB /.*., (Stuiver and Reimer, +33-) using IntCal*.
(Reimer et al., ,**.).
b) Calibration age based on Fairbanks calibration program (Fairbanks et al., ,**/).

At this outcrop, the Za-To + tephra layer has thesmallest thickness (ca.῎. cm), while the Za-To ,tephra layer is thickest (ca. .2 cm) with the Za-To - and. tephra layers having intermediate values (ca.῎2 and,/ cm). Thicknesses of the loess between Za-To + and,, , and -, and - and . tephra layers are ca. +., -+ and+0* cm, respectively. Za-To + tephra presents as lenses,
while Za-To , to . tephras present as stratiﬁed layer.
However, Za-To - tephra sometimes presents as discontinuous layer. The Za-To , tephra layer is divided into
lower, middle, and upper parts. The thicknesses of these
are ca. ., / and -3 cm at Loc. 1, respectively. The upperand lower parts are composed of scoriaceous volcanic
sands, while the middle layer is composed of red colored
scoria only. Itagaki et al. (+32+) named the red colored scoria the Zao Kawasaki scoria (Za-Kw).
In addition, a gravel layer is sometimes observed
below the Za-To + tephra layer. The thickness of theloess lying between them is ca. .* cm. The gravel layer
is composed of subangular to subrounded gravel lessthan , m in diameter, and poorly sorted. It is considered that the gravel layer can be correlated to subangular to subrounded gravel layer which was describedby Itagaki et al. (+32+). Itagaki et al. (+32+) reported
that the radiocarbon age of wood sample from subangular to subrounded gravel layer which was obtainedat the other location is -+,/** ῌ,,0+*/῍+,31* yr BP.
Isopach maps of Za-To + to . tephra layers are shownin Fig. +. They are distributed mainly on the east
downwind side. Isopach maps show that these tephras
originated from the Zao volcano. The main axis of
Za-To + to . tephras extend toward the east-southeast,
east-northeast, east and east-northeast, respectively.
-. Radiocarbon age
The representative columnar sections are shown in
Fig. +. At Loc. 1, the reddish-dark brown colored
paleosol (῎, cm thickness paleosol parts) is observed infour horizons, just above the top of the gravel layer andjust below the bottom of Za-To ,, - and . tephra layers(Fig. +). We sampled the paleosols from these horizons for radiocarbon dating. The material of samples+1ῌ*,, +1ῌ*- and +1ῌ*. passed through a *.+ mm sieve
was stirred by an ultrasonic cleaner, and puriﬁed by acidtreatment. The pretreated material was oxidized byheating at 2/*῏ together with CuO. The produced
CO, was reduced catalytically to graphite on Fe-powder
with hydrogen gas at 0/*῏. For these three samples,
we used an AMS system at the Paleo Labo Co., Ltd to
make radiocarbon measurements of graphite targets
with NIST OX-II as standerds. The material of sample+1ῌ*+ was puriﬁed by acid and alkali treatments. The
pretreated material was oxidized by heating in a vacuum
together with CuO. The produced CuO was reduced
to graphite using the method of Kitagawa et al. (+33-).
For this sample, we used a Tandetron AMS system at
the Tono Geoscience Center to make radiocarbon measurements of graphite targets with NIST OX-II as standards.
The results are shown in Table +. Radiocarbon ages
were corrected by d +-C and calculated using a Libby
half-life of /,/02 years. The well known radiocarbon
age calibration curve IntCal*. (Reimer et al., ,**.)
extends back to ,0 cal kyr BP, however the calibration
curve spanning ,0 to /* cal kyr BP is tentative (van derPlicht et al., ,**.). The age of the sample +1ῌ*. wascalibrated by the calibration program CALIB /.*.,(Stuiver and Reimer, +33-) using IntCal*. (Reimer etal., ,**.), but the other three samples were calibrated
by Fairbanks calibration program (Fairbanks et al.,,**/) (Table +), because these three ages are out ofrange of the IntCal*.. The calibrated calendar ages
are used in the following discussion. It is consideredthat the radiocarbon ages of the samples +1ῌ*,, +1ῌ*and +1ῌ*. are equivalent to those of the nearby tephra
layers. Because the radiocarbon dates paleosols underlying tephra layers, can represent the eruption age(Okuno, ,**+). Thus, the ages of the Za-To , to .
tephra layers are deduced to be ca. -*.1, ,1.+, and +,.3
cal kyr BP, respectively. The radiocarbon age of the154

Kotaro MIURA, Masao BAN and Hiroshi YAGI
Table ,.

Representative compositions of volcanic glasses in L-+ to 0.

FeO*, total iron calculated as FeO.

sample +1῍*+ is in the range of the error bar of that ofa wood sample from the gravel layer which was reported
by Itagaki et al. (+32+).
The sedimentation rate of loess is considered to berelatively constant in a ﬂat area (Hayakawa, +33/) suchas Loc. 0 and 1. Using the obtained ages of Za-To , to
. and the thickness of the loess between them, the rates
during Za-To , to -, and Za-To - to . tephra layers arecalculated to be similar value of ca. *.*1 mm/yr at Loc.
0. At Loc. 1, those are calculated to be ca. *.*3 and*.++ mm/yr, respectively. The rate during the sample
no. +1῍*+ loess horizon to Za-To , tephra layers is also
calculated to be *.*3 mm/yr. These values are in therange of the sedimentation rate of the loess in Japan(*.*.῍*.+/ mm/yr) reported by Hayakawa and Yui(+323). Using the obtained rates, the age of Za-To +tephra layer at Loc. 0 and Loc. 1 are calculated to be ca.
-- and -, ka, respectively. The age of the Za-To +tephra layer would be some time between ca. -- and -,cal kyr BP.
.. Volcanic glasses in the loess
We re-examined the volcanic glass shards in the upper
part of the loess below the Za-To . tephra where volcanic glasses were reported by Imura (+330).
At Loc. 1, we collected six samples (L-+, ,, -, ., / and0) from the upper part of the loess (0* cm in thickness)below the boundary with the Za-To . tephra layer.
Samples L-+ to 0 were collected from the loess at 0*῍/*
to +*῍* cm from the boundary (Fig. +). The samples
were washed by an ultrasonic cleaner, dried in an ovenat 0*ῌ, and sieved. Volcanic glasses obtained in therange of *.*22῍*.+,/ mm were used for microscopeobservation and chemical analysis. Knowing the chemical composition of the volcanic glasses is very usefulwhen identifying the widespread tephras. The chemical compositions of the glasses were undertaken with a
JEOL 20**M electron microprobe at Yamagata University using a wavelength-dispersive technique. Operating conditions were +/ kV accelerating voltage, *.*+ mA
beam current and a +* mm defocused beam. Analyses
were corrected using the oxide ZAF method.
Under the microscope, most of the volcanic glass
shards shape in L-+ to 0 are the pumice type (Machida
and Arai, ,**-), while a small number of volcanic glass
shards in L-- to 0 are the bubble wall type (Machida
and Arai, ,**-). Representative compositions of volcanic glass shards in L-+ to 0 are listed in Table ,. All
discussion here refers to analyses that have beennormalized to +**ῌ volatile free with total iron (FeO*)
calculated as FeO. Representative major elements vs.
SiO, diagrams are shown in Fig. ,. Data from the AT

The Tephra Layers Distributed around the Eastern Foot of the Zao Volcano

155

and To-H (To-HP) (Towada-Hachinohe tephra) by
Machida and Arai (,**-) are also shown in Fig. , forcomparative purposes, because these two are the potential candidates among widespread tephras to have deposited in Zao and the surrounding area during ca. -,῍+, ka. To-H (To-HP) was discharged from the Towada
caldera, with an estimated age of ca. +../῍+1 ka. It is
widely distributed mainly around the northern part of
NE Japan. The shape of volcanic glasses is the pumicetype (Machida and Arai, ,**-).
The silica contents of the volcanic glass shards (L-+to 0) ranged from 1/ to 2* wt.ῌ. In the K,O vs. SiO,
diagram, the volcanic glass composition is split into twogroups. One group has low K,O (+.+῍+.2 wt.ῌ) content with a range of 1/῍2* wt.ῌ SiO,, and the other hasa high K,O (,.-῍/.- wt.ῌ) content of 11῍2* wt.ῌ SiO,.
All of the bubble wall type glasses, which were found in
L-- to 0, belong to the latter group, and the plotted areaof this type of glass is similar to that of AT glasses in theK,O vs. SiO, diagram as well as in the other SiO, variation diagrams (Fig. ,). The low-K,O glasses can bedivided further into lower (1/῍12 wt.ῌ) and higher(12./῍2* wt.ῌ) SiO, groups. The glasses of formergroup were from L-, to 0, and the compositional rangeof this group is in the To-H (To-HP) ﬁeld in the K,O vs.
SiO, diagram as well as in the other SiO, variation
diagrams. Volcanic glasses of the high-K,O pumicetype and low-K,O · higher SiO, group have di#erent
compositions from either of the AT and To-H (To-HP)
glasses. It is probable that they were derived from thevolcanoes in and around the Zao area.
Consequently, AT and To-H (To-HP) volcanic glasses
were found in L-- to 0 and L-, to 0, respectively. The
age of L-, is calculated to be ca. +1.2῍+0.2 ka, using thesedimentation rate of the loess which was obtained in
the previous section. The value is comparable to theage of To-H (To-HP) by Machida and Arai (,**-).
Therefore, it is considered that the AT and To-H
(To-HP) volcanic glasses found in the L-- to 0 horizons
have a reworked origin and the To-H (To-HP) volcanic
glasses were deposited as near primary tephra in the L, horizon and show the age of the loess.

Fig. ,. SiO, variation diagrams for volcanic glasses. FeO*
῎total iron calculated as FeO. Solid and broken
envelopes show ﬁelds of the AT and To-H volcanic
glasses, respectively (Machida and Arai, ,**-).

/. Discharge rate
Discharge volumes of Za-To + to . tephra layers were
estimated using an empirical formula proposed by
Hayakawa (+32/). The formula is V῎+,.,TS where
V is the discharge volume, T is a certain thickness, andS is the area enclosed within the isopach of thickness T.
Volumes of Za-To + to . tephra layers are ca. -῍+*ῌ,,-῍+*ῌ+, +῍+*ῌ+ and +῍+*ῌ+ DRE km-, respectively(Table -).
A magma-discharge stepdiagram during the Za-To +to . activities, using the volumes and the ages of thetephras obtained in this study, is shown in Fig. -. The

156

Kotaro MIURA, Masao BAN and Hiroshi YAGI

Table -. Discharge volumes of Za-To + to . tephras.
Densities were determined using weight of a +**ml beaker ﬁlled with the tephra which was driedin an oven at +*/῎.

-῍+*ῌ,, -῍+*ῌ+, +῍+*ῌ+ and +῍+*ῌ+ DRE km-, respectively and the averaged discharge rate during Za-To+ to . is calculated to be *.*,ῌ*.*- km-/ky.
Acknowledgements
Many constructive comments and suggestions fromDr. M. Okuno of Fukuoka University, Dr. T. Oikawa ofGeological survey of Japan, and the editor Dr. D.
Miura of Central Research Institute of Electric Power
Industry greatly helped to revise the manuscript. We
are grateful to Dr. R. W. Jordan for correcting theEnglish in this paper. This work was ﬁnancially
supported in part by Grant-i-Aid for Scientiﬁce Research (no. +1/.*./+) from the Japan Society for the
Promotion of Science to M. Ban.
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Fig. -. A magma-discharge stepdiagram during Za-To+ to . tephras.

intervals of Za-To + to , (ca. ,.-ῌ+.- ky) and Za-To , to
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discharge rate during Za-To + to . is calculated to be ca.
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origin, the To-H (To-HP) glasses were deposited asnear primary tephra.
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