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LATE CENOZOIC OROGENY IN JAPAN
T. MATSUDA,
K. NAKAMURAI
IEarthquake Research Institute,
keological
Institute, University
(Received
November
and A. SUGIMURA2
University
of Tokyo,
of Tokyo (Japan)
Tokyo (Japan)
7, 1966)
SUMMARY
Late Cenozoic tectonic maps are serially given to show the amount of
vertical displacement since Miocene, trends of fold axes and degree of deformation of sedimentary rocks in Japan. They illustrate some differences
between the east Japan and west Japan arc systems. Lines of evidence show
that the former is more active.
In the east Japan arc system a series of erogenic events started at the
beginning of the Miocene. The trend of the Late Cenozoic erogenic belt is
discordant with those of Mesozoic erogenic belts. The younger orogeny
seems to be genetically independent of the older ones, although the older
structures have given some effects on the younger ones in central Hokkaido
and in south Fossa Magna. The east Japan arc system consists of the inner
volcanic, outer geanticlinal and outermost subsiding trench belts. The inner
and trench belts are regarded as forming a pair of high-temperature and
low-temperature tectogenic belts. This pair may correspond to that of the
Mesozoic erogenic belts as revealed by the study of metamorphic facies
around the Pacific.
INTRODUCTION
During the last ten years, since Ikebe (1956) compiled the Cenozoic
history of Japan, and Minato et al. (1956) summarized Tertiary history of
east Japan from the viewpoint of structural geology of the island arcs, the
studies of the Late Cenozoic geology and the geophysical features of Japan
have been much advanced by many Japanese scientists. Based on these
studies, the main geologic events during the Late Cenozoic in Japan are
summarized here and the island arc features are discussed as an expression of a recent erogenic activity, considering a regular.pattern of regional
metamorphism in the circum-Pacific
older erogenic belts.
This paper is the second report on the Late Cenozoic orogeny in Japan,
the first one being mainly concerned with volcanic materials (Sugimura et
al., 1963).
In preparation of this paper, the authors are indebted to many excellent
reports concerning geology of the Japanese islands, including those by
petroleum geologists (Hashimoto, 1962) and recent synthesis of the geology
Tectonophysics,
4(4-6)
(1967) 349-366
349
::*@?
b
Fig.1. Island arcs in Japan. Pair of stippled and vertically hatched
areas = Late Cenozoic erogenic belts; horizontally hatched area = MeeozoicTertiary geosynclinal belts; H = Hidaka erogenic belt; S = Shimanto Belt.
350
Tectonophysics,
4 (4-6) (1967) 349-366
of Japan (Minato et al., 1965), especially to geologic sheet maps of
1:50,000 and other scales published from the Geological Survey of Japan.
NEOTECTONIC
DIVISION
OF THE
JAPANESE
ISLANDS
The Japanese islands consist of’ several island arcs (Fig.1). They are
grouped into two island arc systems; the east Japan island arc system and
the west Japan island arc system.
The east Japan arc system shows not only a distinct zonal arrangement
in distribution of deep-seated earthquakes, gravity anomalies, volcanoes,
nature of volcanic rocks, are topography (Sugimura, 1960) and terrestrial
heat flows (Uyeda and Horai, 19641, but also a series of tectonic movements
in Late Cenozoic time, which would be regarded as erogenic processes.
The west Japan arc system, on the other hand, is less active in general
than the east Japan system. Particularly, the fundamental arc-structure
of
the southwest Honshu Arc had been constructed before the Miocene, and zonal
arrangement of geophysical phenomena such as that observed in northeast
Honshu Arc is less distinctly recognized at present. The southwest Honshu
Arc would be older than the northeast Honshu Arc.
The northeast Honshu Arc is divided into three tectonic provinces; the
inner volcanic belts, the outer non-volcanic geanticlinal belt, and the outermost subsiding trench belt.
The volcanic and oil field region, or the so-called
green tuff region”
onthe Japan sea side, belongs to the inner belt, and the Kitakami-Abukuma
region on the Pacific side belongs to the outer belt. The third belt lies off
Honshu, including the Japan Trench.
The east Japan arc system obliquely crosses the older erogenic belts.
In the central part of Hokkaido, the east Japan arc system intersects the
Hidaka erogenic belt which is similar in age to the Alpine orogeny in Europe.
In the south Fossa Magna region of central Japan, the inner belt of the east
Japan arc system superimposes upon the Shimanto Belt, which is an outer
geosynclinal belt of Mesozoic to Paleogene orogeny in southwest Japan. In
the above two regions, the structure of Late Cenozoic formations is more
or less controlled by the older orogeny.
OUTLINE
OF NEOGENE
SEDIMENTARY
HISTORY
OF HONSHU
During Early Tertiary time, most of the Japanese islands had been
subjected to subaerial denudation, However, two geosynclinal belts, the
Hidaka Belt (Hunahashi, 195’7) in central Hokkaido and the Shimanto Belt on
the Pacific side of southwest Japan, have existed since Mesozoic time.
Toward the beginning of the Miocene, the Japan Sea side area of
Honshu became suddenly a region of violent volcanism followed by regional
subsidence. The subsidence culminated during Middle Miocene, Afterwards,
the sea has gradually retreated in general.
Fig.3 is a schematic diagram showing sedimentary history of the northeast Honshu Arc. Deposition in the inner belt started in the Early Miocene
on basement rocks of Paleozoic formations and Late Mesozoic granites, with
the accumulation of volcanic material, mainly of andesite and dacite of
Tectonophysics, 4
(4-6)
(1967)
349-366
351
1
NEOOENE ANO
QUATERNARYROCKS
m
MOOENE
ORANIlE
PRE-NEOEENE
-S&lhMaw
PK- ,Fosra
*
352
*cc
G
Tectonaphyeics, 4 (4-6) (1967). 349-366
alkaline, high-alumina basalt and tholeiite series (Ozawa, 1963; Miyagi,
1964), which were laid down partly on land and partly under sea water.
These volcanics were covered by marine, rather uniform, oil-producing
mudstone of the Middle Miocene age. The volcanism of basalt and dolerite
was characteristic
in this stage, along with acidic volcanism.
After the extensive deposition of marine mudstone in the Middle
Miocene, differentiation into a few rising zones and downwarping basins
began. The trend of arrangement of these zones and basins is parallel to the
present northeast Honshu Arc. The sinking basins became narrower towards
the end of the Miocene. In Pliocene time, they were separated into several
intermontane, lacustrine basins (Kitamura, 1959; Ikebe, 1962). These basins
and intervenient mountains correspond well, in situation, to the present-day
basin and range topography in northeastern Honshu.
Accompanying the differentiation of the basins in the inner belt,
granitic intrusions occurred in upwarping areas, The areas of marine
sedimentation still remained in Pliocene but were restricted along the
present coast.
In contrast to the inner belt, the outer belt of the same arc, the
Kitakami and Abukuma Mountains, have kept a rising tendency with block
movements during the Late Cenozoic (Chinzei, 1966).
The southwest Honshu Arc, on the other hand, has been less mobile in
general, but there are structural provinces arranged parallel to the trend
of the southwest Honshu Arc (Cenozoic Research Group of southwest Japan,
1960). The Japan Sea coast area (Hokuriku-San’in area) is similar in Miocene
history to the inner belt of the northeast Honshu Arc in having Early Miocene violent volcanism and the succeeding marine invasion (Matsumoto and
Wadatsumi, 1959; Kaseno et al., 1961; Sakamoto, 19661, whereas the Pacificside belt (Nankai area) was entirely different in tectonic condition from the
outer (Pacific-side)
belt of the northeast Honshu Arc. The Nankai area had
still been subsiding in Early Miocene as well as in Early Tertiary times,
as a part of the Shimanto geosyncline. The median belt (Setouchi area) of the
southwest Honshu Arc (Huzita, 2962) was the area of depression in Miocene
and again in Pliocene, where thin shallow-sea deposits (Miocene) and
lacustrine deposits (Pliocene) were formed. Since Pliocene, upwarping and
block movement in meridional trend have become remarkable over the eastwest trend of Miocene movements.
Fig.4 is a summary of chronological change of marine invasion (the
third column), volcanic activity (the fourth column), and assumed intensity
of crustal deformation (the fifth column) in the Japanese islands. The figure
suggests some interrelationship between tectogenesis and volcanism.
TECTONIC
DEFORMATION
SINCE MIOCENE
Fig.5 shows the distribution of vertical displacement since the beginning of the Miocene. The total amount of vertical displacement of the ground
surface is assumed to be represented by the present height of basal unconformity of marine Miocene deposits. For upheaved areas where the Miocene
deposits were either completely eroded out or, not deposited, the amount was
estimated from the altitude of nearby mountains capped by the Miocene
deposits or from the data on Quaternary tectonic movement (Hatori et al., 1964).
Tectonophysics, 4 (&S) (1967) 349-366
353
AQUITANIAN
BURDIGALIAN
VINDOBONIAN
SARMATIAN
1
PONTIAN
PLEISANCIAN
7
PLEISTOCENE
STANDARD
EUROPEAN
ONNAGAWA
VOLCANIC
BASIC VOLCANIC
ACIDIC
Y""
I
I
ROCKS
ROCKS
PENINSULA
OGA
t-W
7;
DAISHIMA
---_
NISHIKUROSAWA
m---w_
FUNAKAYA
.------
KITAURA
WAXIMOTO
------
SHIBIKAWA
.-----
KATANISHI
STANDARD
OF
N.E. HONSHU
I
g
VI
OILFIELD
AKITA
DEWA
SILICEOUS
SILTSTONE
SANDSTONE
MARINE
YOXOlE
BELT
SHALE I
CONGLOMERATE
INNER
DEPOSITS
5l.l
i5U
NON-\1ARIM
KITAKAMI
E-
t'I.ASTi-c
DEF'O~II'
MOUNTAINS
BELT
KITAKAMI
OUTER
Subsidence prevails in the inner belt of east Japan, where the depth of
the Miocene base attains more than 5,000 m in some basins.
The trend of individual basins in the belt, however, is diagonal to the
arc.
Most of the central zone of the Hidaka erogenic belt and the outer belt
of the northeast Honshu Arc belong to the area of upheaval. Southwestern
Japan shows a relatively uniform tendency of uplift, but local displacement
is fairly remarkable as described by Huzita (1962). The mountains in central
Japan are inferred to have uplifted 2,000 m or more in amount.
Neogene rocks, even Quaternary rocks in places, are folded to various
degrees. Fig.6 shows distribution of the general trend of fold axes. One
linear mark indicates the average direction obtained from fold structures
with wavelength about several kilometers in a sheetmap area of about 24 X 19
km2. The smaller map in Fig.6 shows folded zones of Japan and their general trend. Generally, these directions of folding are parallel to the trend
of the present arcs (Fig.lf, but are not concordant with those of older rocks
except in central Hokkaido and in south Fossa Magna (Mats&a, 1962), where
the trend of Late Cenozoic folds is nearly parallel to the older belts and the
Early Miocene rocks are folded together with Paleogene and older rocks.
Fig.7 shows the distribution of the degree of deformation since Miocene
times, calculated from geologic sections mostly of the scale 1:50,000. Here,
the degree of deformation is defined as a sum of the vertical component of
folded strata and of the throws of faulting, CAH, divided by a length L, of the
geologic section. Contour lines were drawn, based on the weighted means of
degree of deformation obtained from the adjacent three or four points.
Through this process,
local high values partly due to a shorter L, less
than about 10 km, are levelled. One of highly deformed zones lies in the
Japan sea-side area of Honshu and Fossa Magna of the inner belts of
the east Japan arc system. Another zone in Hokkaido is nearly parallel
to Hidaka erogenic belt and is thought mainly to be the product of the
late stage of the Hidaka orogeny.
Most foldings in the folded zones of east Japan are still active. This
is indicated by folded Quaternary strata, folded river terraces and by precise
re-levelling (Otuka, 1941; Sugimura, 1952).
A folded zone running along the Pacific coast of southwest Japan is
older and is not active, There, the non-folded post-Early Miocene deposits
cover the folded Miocene and earlier strata, forming gentle broad half-basin
structures.
On the basis of previously obtained data about the time rate of deformation for the past 10’ years, the age of commencement is inferred by some
active deformation observed at the places shown in Fig.8. Here, the last high
sea level (Shimosueyoshi stage) is assumed to be about 9.10* years ago.
The known rates used here are of the order of 0.1-9.5 km/105 years for
vertical and horizontal displacements and 1o-2o/1O5 years for folding and
tilting. If the rate of deformation is taken as constant during recent geologic
time, the deformation in the areas mentioned should have started one to a
few million years ago f Fig.8) (Sugimura, in press).
Fig.3. Stratigraphic columns of sedimentary basins in the northeast
Honshu Arc (Chinzei, 1967). Numerals in columns indicate thickness in
meters.
Tectonophysics, 4 (4-6) (1967) 349-366
355
VOLCANIC
ROCK
I)EFO~TI~
04krn3/rn? INCREASINc
RATJ
3
PIEISTOCENE
I KATAN'ISHI
1
I
SHIBIKAWA
-
PLIOCENE
IUmKTWOTO!
KITAURA
10 -
l----i
FUNAKAWA
ONNAGAWA
I
20 NISHIKUROSAWA
Y
A
'X
,
,
I
after
KITAMURA
(1959)
x IKEBE
11962)
MINATO
A
ifter
SUGIMURA
et aL
(1963:
l
et al.
Fig.4. Ratio of emerged area to invaded area for northeast Honshu,
volcanic material erupted on main islands and inferred rate of deformation
in the stages since Miocene.
356
Tectonophysic5,4 (4-6)(1967)349-366
e
/
+
loaom
i._.
0
g&“-
y,,,
-
-3000
-
-5000
Fig.5, Distribution of vertical displacement since the Miocene. The
smaller map indicates the points where the heights of ~n~~~~rrn~~y were
estimated,
Tectonophysics, 4 {4--6) (1967) 349-366
357
c
141*
i
-f32%
l34O
O-
ZOOKM
Fig.6. Trend of fold of Neogene rocks. Hatched areas are pre-Neogene
rocks.
358
Tectonophysics,
4 (4-6)
(196’7) 349-366
I4 2"
,4b0
/
i
_--
42.
_---
2
-
!
i
I
I
^_
El
-
0
general
Fig.7. Degree
distribution
Tccronophysics.
of deformation
since the Miocene;
of highly deformed
area.
4 (4 -6) (Iy6i)
34% 366
-
ZOOKM
smaller
e
(I
a
0.6
0.8
1.0
map shows
359
pzI@c)oS
Of
UmmwHI
A
Fig.8. Inferred durattion of deformation under the assumption of constant rate. A. Verticaland
horizontal movements.
B.Tflting due tofolding
in east Japan. Horisontal lines indicate the amount of observed or possible
maximum displacement
at each area. Oblique lines show the constant time
rages of respective deformation estimated for recent geologic time (within
10” years). The cross points of the horizontal and the oblique lines indicate
the inferred age of beginning of the deformation in respective area - after:
Sugimura and Matsuda (1965) for the Atera fault; Sugimura and l&ruse (1865)
for Nozima-zaki;
Yoshikawa et al. f 1964) for Muroto-zalci; Matsuda (1986)
for the Atotsugawa fault; Nakamura et al. (1965) for Awashima;
Nakamura (1957) for Ojiya; Sugimura (1967, in press) for Ogurd.
Activation of tectonism since Late Pliocene is actually pointed out in
some areas (Huzita, 1962; Chinzei, 1966; Matsuda, 1966). These suggest that
the neotectonic movement in Japan might have been accelerated
since Late
Pliocene as compared with that in Miocene (Fig.4). This suggestion is a
problem to be examined further.
360
Tectonophysics,
4 (4-6) (1367) 349-366
0.1
10nr
I
PERfODS
OF
DURATION
B
Fig.BB
ISLANDARC
(Legend see p. 360).
FEATURESANDOROGENY
Schematic cross section across the northern part of the northeast
Honshu Arc is illustrated in Fig.9, and the characteristic features of geology
are compared between the inner, the outer and the trench belts of the arc
(Table I).
The trench belt of the arc is characterized by strong negative gravity
anomalies, low heat-flow values and high mantle seismicity. The belt has
subsided during Late Cenozoic, particularly since Late Pliocene (Iijima and
Kagami, 1961). The active tectonic state of the belt is also suggested by thick
young sediments and young faulting (Ludwig et al., 1966).
The outer belt corresponds to the non-volcanic outer arc of the double
arc (Umbgrove, 1947). The outer belt of northeast Honshu Arc consists
mostly of metamorphosed Paleozoic rocks and Mesozoic granite and
sedimentaries. This belt has been rather stable and has slowly uplifted
throughout Cenozoic time. Raised peneplains are present. Late Cenozoic
sediments are scarce and remain unfolded, dipping gently toward the sea.
Volcanism is essentially absent during Cenozoic time.
The inner volcanic belt, on the contrary, has been the region of violent
volcanism and rapid sedimentation in late Cenozoic time. History of events
Tectonophysics, 4 (4-6)(1967)34S-366
361
0
/
2OOkm
Fig.9. A schematic profile across the northern part of the northeast
Honshu Arc. HF = heat flow (Uyeda and Horai, 19641, G = gravity (Bouguer
anomaly for land, Tsuboi et al., 1956; free air anomaly for sea, recalculated
by Sugimura, 19601, T = topography, E = foci of mantle earthquakes.
TABLE I
Characteristic geologic features of the inner, outer and trench belts of the east Japan
arc system
Inner belt
Outer belt
Intermediate to acidic
volcanism with granitic
intrusion
essentially no
volcanism
Local vertical movements
resulting in basins and
mountains
gentle, continuous
upwarping
regional subsidence
and accumulation of
sediments, particularly
since Pliocene
Moderate folding
no regional
folding
probable strong folding
and faulting
Alteration or metamorphism,
producing: zeolite, chlorite,
epidote albite etc., in
volcanic rocks.
362
Trench belt
possible regional
metamorphism of highpressure, low-temperature
tvoe
Tectonophysics, 4 (4-6) (1967) 349-366
and structural trend are not inherited ones from the older orogeny, but are
thought to be originated at the beginning of Miocene. This belt is composed
of oil-bearing, moderately folded sedimentary basins and volcano-capped
upraised ranges. Acidic to intermediate volcanism has repeatedly occurred
since Miocene. Granitic plutons are associated with them (Fig.2). Miocene
volcanic rocks often show a greenish appearance, due to alteration
products
such as epidote, chlorite and other clay minerals (so-called
“green tuff”).
Mineral assemblages of zeolite facies and those similar to greenschist
facies are present in the inner belt of the arc (Yoshimura, 1961; Utada, 1965;
Shimazu and Sato, 1966), The metamorphic series from the zeolite facies to
greenschist facies through the pumpellyite-prehnite
metagraywacke facies,
has been found in this belt from the South Fossa Magna region (Sakamoto et
al., 1964; Matsuda and Kuriyagawa, 1965), where the Shimanto Belt extends
across the inner belt of the east Japan arc system.
The problem whether or not the east Japan Arc system can be regarded
as a modern erogenic belt independent of the older one, is discussed as follows:
The Cenozoic events in Japan had been taken as post-erogenic
disturbances following the Mesozoic orogeny. In 1956, however, Minato et al. compared the whole Late Cenozoic history of the inner belt of east Japan arc
system with a life of an orthogeosyncline which had the initial, syn-erogenic,
and final volcanisms in terms of Stille (1940). Two years later, Sugimura
(1958) stated that recent-tectonic activities in the east Japan arc system including the outermost trench belt were probably the expression of a new
orogeny started in the Miocene. In 1961, Miyashiro (1961a,b) suggested a
possibility that the trench belt and the inner belt along the island arc correspond to the present-day metamorphic belts of high-pressure,
lowtemperature type and low-pressure,
high-temperature type, respectively.
This idea was followed by Matsuda (1964) in his review of the tectonic state
of the Japanese islands and further supported by Takeuchi and Uyeda (1965)
who examined the terrestrial heat flow data along the east Japan arc system.
As stressed by Miyashiro (1961a), most of the Mesozoic erogenic belts in
the circum-Pacific
region have a pair of metamorphic belts of contrasted
characters, viz. I0the inner metamorphic belt” on the continental side, and
“the outer metamorphic belt” on the oceanic side. The concept of a paired
belt in metamorphic terrain can be extended to the erogenic belt in general,
namely, the erogenic belt can be regarded as consisting of “the inner oroTABLE
II
Contrasted features of paired erogenic
Inner erogenic
belt
belt
Outer erogenic
belt
(Geosynclinal
subsidence
is
not necessarily
accompanied)
geosynclinal
subsidence
and thick
accumulation
of sediments
Intermediate
to acidic
magmatism
(“syn-0rogenic
and subsequent volcanism”)
basic and ultra-basic
(ophiolitic)
magmatism
(“initial magmatism”)
High-temperature,
low-pressure
type metamorphism
strong deformation
of sediments
and regional metamorphism
of highpressure
low-temperature
type
Tectonophysics,
4 (4-6)
(1967) 349-366
363
genie belt” and “the outer erogenic belt”. Essential
features
of the inner and
the outer erogenic belts are summarized
in Table II.
“Late Cenozoic orogeny ” , has not been fully accepted,
because much attention has been paid only to the inner belt of the east Japan arc system,
Indeed, the inner belt alone is not enough to be regarded as an erogenic belt.
But, from the similarity to the Mesozoic orogeny in the Pacific region, it
would be concluded that the Late Cenozoic island arc systems in Japan and
also other active island arcs around the Pacific, probably represent new
paired erogenic belts now in action.
The inner volcanic belt of the modern island arc would correspond to
the inner erogenic belt, and the outermost subsiding trench belt would correspond to the outer erogenic belt of the circum-Pacific-type
orogeny.(The
outer geanticlinal belt of the island arc may have no corresponding belt in
the Mesozoic erogenic belt, as in case of a single-arc type of the present
island arc where the outer geanticlinal belt is absent)
ACKNOWLEDGEMENTS
The authors are much obliged to Prof. Tatsuro Matsumoto of the
Kyushu University, who encouraged them to prepare this paper. Thanks are
also due to Prof. Fuyuji Takai of the University of Tokyo, under whom this
work was begun. The authors are very grateful to Dr. Kiyotaka Chinzei of
the University of Tokyo, who always joined the constructive discussion and
contributed much to this paper,
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L. Krasny (U.S.S.R.):
I am interested in the outermost trench belt. Is it the process of oceanization
or
continentalisation?
The fracture zone discovered
by Udfnteev, several hundreds of
kilometers
to the east of the Kurile-northeast
Japan Arc, may be the beginning of a
future mobile belt. Do you think so?
T. Matsuda (Japan):
The subsiding character
of the outermost
trench belt is thought to be an orogenie feature displayed only in the erogenic time. In the post-erogenic
time after the
subsidence,
the belt would be upraised and exposed along the outside of the older
continental crust as a granite-free
eugeosynclinal
belt similar to the Shimanto Belt
of southwest Japan or the Franciscan
Belt in California.
This is not a procees of
oceanization.
Udintsev’s
discovery
is very interesting,
but owing to my lack of knowledge concerning
it, I feel unable to discuss the tectonic meaning at present.
366
Tectonophysics,
4 (4-6)
(1967) 349-366