explanatory text of the quaternary tectonic ......explanatory text of the quaternary tect0nic map of...
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EXPLANATORY TEXT OF THE
QUATERNARY TEcT0NIc MAP OF JAPAN
P”〃ゐ加〃〃加1Wゴo”〃R2醐κ”α”〃伽肋伽2〃κ〃”〃o”
胴舳〃〃肋〃010馴■8舳ツ 1bκγo， ハ伽”c” 1973
551．24：551．79（52）
Exp1amatory Textof t11e Quatermary Tectomic M叩ofJa脾m By
The Rese趾ch Gr㎝p for Q㎜tem肚y T㏄t㎝ic M叩，Tokyox
Abstmct
The Quatemary Tectonic Map of Japan，compiled by the Research Group for
Quatemary Tectonic M叩and pub1ished by theNationa1ResearchCenterfoIDisaste正Prevention in August1969，consists of the fol1owing six sheets．
No．1－Vertical disp1acements estimated with geomorpho1ogica1method．
No．2．Vertica1disp1acements estimated with geo1ogica1method．
No．3．Vertical disp1acements compi1ed from the maps Nos，1and2．
No．4．Distribution offau1ts．
No．5．Distribution offolds．
No．6．Gipfe1nur．
The Map No．1shows the present heights of the erosion f1at surfaces formed
during the1atest Tertiary or the ear1iest Quatemary age．In producing this map，it is
assumed that the erosion surfaces were foエmed not far from the sea1eve1．The map No．
2shows the present altitudes and the depths of the locations where upper P1iocene to
1ower Pleistocene marine sedimentary formations crop out or are buried．The amounts
of vertica1disp1acement estimated by geo1ogica1method are considered to represent
the tota1amounts of the crusta1movement from the beginning of the Quatemary to
the present．Errors which are derived from the assumptions that the sedimentation
occured at sha11ow depths are neg1ected because of the next reasons．
1t is not a1ways possib1e to determine exactly the P1io－P1eistocene boundary in
the sediments and it is often ob1iged to take the depositiona1surfaces oエthe erosion
surfaces which may have considerab1e time gaps．
1n the map No－1，the amount of up1ift can be traced regiona11y，but the amount
of subsidence can not be known．In the map No．2，both the amounts of uphft and
subsidence can be known but they can be determ㎞ed on1y1oca11y．Tak㎞g advantage
of the two mehtods，the authors synthesized the map No．3，which is one of the
conclusions of this work．
＊ Kenzo Hatori，Jindai High Schoo1，Tokyo；Ryoji Ishii，Hakuo High School，Tokyo；
Sohei Kaizuka，Tokyo Metropolitan University；Chosei Komori，Musashi High
Schoo1，Tokyo；Yo Namse，Osaka University of Economics；Yoko Ota，Yokohama
Nationa1University；Fumitake Shimizu，Nationa1Research Center for Disaster
Prevention，Tokyo；Arata Sugimum，＊＊University of Tokyo；Hiroshi Takahashi，柵
National Research Center for Disaster Pエevention，Tokyo；Matsuo Takahas㎞，
Nationa1Research Center for Disaster Prevention，Tokyo；Nobuyuki Yonekura，
University of Tokyo；Torao Yoshikawa，＊＊University of Tokyo．
榊A1l communications conceming the present Text should be addressed to H．
Takahashi，A．Sugimura，or T．Yoshikawa．
H．Takahashi：Nationa1Research Center for Disaster Prevention 15－1 Ginza
6－chome，Chuo－ku，Tokyo 104≡A．Sugimura，Geo1ogical Institute，Facu1ty of
Science，The University of Tokyo，Hongo，Tokyo113；T．Yoshikawa，Department
of Geography，Facu1ty of Science，The University of Tokyo，Hongo，Tokyo113．
一1
Both of the fau1t distribution map（No．4）and the fo1d distribution map（No．5）
aエe drawn foエsuch fau1tings and fo1dings that have deformed sedimentary beds and
terrace suIfaces since the upper P1iocene age．Fau1ts more than1km in1㎝gth and
fo1ds500mto30kminwave1engthareselected． Genera11y speaking，mountain districts have been uplifted，whi1e1ow1ands have
subsided，The maximum up1ift of about1700m is found in the Centra1Mountains
and the maximum subsidence of about1400m in the Kanto Plain（No．3）．It is
conc1uded that the present re1ief of the Japanese Is1ands is large1y due to the
Quatemary tectonic movements．The regiona1trend of fo1d－axes and strikes of faults
shows a characteristic pattem（Nos．4and5）．The Japanese Is1ands may be divided
into some tectonic provinces by the intensity and natuτe of the Quatemary tectonic
mOVementS．
一2
Comtemts
1．Introduction．
2．Quatemary vertica1disp1acement．
2．1．Amounts ofvertica1disp1acement geomorpho1ogica11y estimated．
2．1．1．Method．
2．1．2．Examp1es．
a．Tohoku District．
（i） The Kitakami Mountains．
（ii） The Abukuma Mountains．
（iii） UetSu area．
b．Chubu District．
（i） UOnuma area．
（ii） Northem part ofNagmo Prefecture．
（iii） The Mikawa High1and．
c．Kinki District．
（i） The Nunobiki Mountains．
（ii） The Yamato High1and．
（iii） The Rokko Mountains．
d．Chugoku District．
e．Kyushu District．
f．References．
2．2．Amounts ofvertica1disp1acement geo1ogica11y estimated．
2．2．1，Method．
2．2．2．Examp1es．
a．Up1ifted areas．
（i） Teshio area．
（ii） Boso area．
（iii） The Rokko Mountains．
（iv）Refer㎝ces．
b．Subsiding areas．
（i） K…mto P1ain．
（ii） 0saka P1ain．
（ii）
（iV）
（V）
（Vi）
Nobi P1ain．
Niigata P1ain．
Is㎞kari and Kus㎞エo P1ains．
References．
2．3．Synthesized map，of vertica1disp1acement．
2．4．Regiona1characteristics of Quatemaw vertica1disp1acement．
3．Quatemary fau1ts and fo1ds．
3．1．Quatemary fau1ts．
3．1．1．Method．
3．1．2．Examples．
a．Atera fau1t．
（i） Atera fau1t scarp．＿＿＿＿＿＿．、＿・・＿…・…・
（五）S・kashitaf・・lts…p1・t．
（iii） Strike－shp fault system．
（iv） References．
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一3
b，Mobara＿0ta㎞area．
（i） Introducti㎝．
（ii） Geo1ogy．
（iii） Fault system．
（iv） References．
c．Matsus㎞ro earthquake fault．
（i） Introduction．
（ii） 0ccurrence．
（iii） Tectonic setting．
（iv）References．
3．2．Quatemary fo1ds．
3．2．1．Method．
3．2．2．Examp1es．
a．Niigata area．
b．Mogami area．
c，The Nemuro Peninsu1a，eastem Hokkaido．
3．2．3．Regiona1distribution．
a．Distribution of antic1inal axes．
b．Relation between rate and wave1ength．
c．Geogmphical distribution of the rate and Quatemary folding areas・
3．2．4，Discussion on the formation of the Quatemary fo1dings．
a．Rate of fo1dings and t㎞ckness of sedimentary rocks．
b．Direction of fold axis and that of compressive stress．
3．2．5．References．
3．3．Regiona1characteristics ofQuatemary fau1ts and fo1ds．
4．Gipfe1flur map．
5．・Discussion．
5．1．Tectonic setting of the Japanese Islands．
5．1．1．Topographica1and geophysical features．
5．1．2．Geo1ogica1stmcture．
5．1．3．References．
5．2．CompaTison with Neogene tectonic movements．
5．2．1．Vertical disp1acement．
5．2．2．Fo1ding or deformation of strata．
5．2．3．Re脆f．
5，214．Conc1usional remarks，
5．2．5．References．
5．3．Comparison with present seismic energy distribution．
5．3．1，Introduction．
5．3，2．Method．
5．3．3．Comparison，
5．3．4，ConclusiOn．
5．3．5．References．
5．4．Quatemary tectonic divisions of Japan．
5．4．1．Method．
5．4．2．Regiona1description．
5．4．3．References．
6．Postscript，
7．ApPen血ces、
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7．1．
7．2．
7．3．
7．4．
7．5．
7．6．
List of the present heights ofgeo1ogic formations．一………・一・・一……………・・一…・・……・…・・…＿ 78
List of drilling．。＿＿、＿＿＿．．．。＿＿＿＿＿＿、．、．＿＿＿＿＿。。．．＿。＿＿＿＿。。。．＿＿＿＿＿．．．．．．．．．．．．．．．．．．．．．．．．．．．．．．．． 112
List of fau1し 118
Li・t・ff・1山 158Abstmcts ofPapers on the Quatema工y Tectonics（in Japanese）．。＿＿＿＿．．。．一。＿．．Another vo1ume
Emta of the Map No・2，Vertica1displacements estimated with geo1ogical method． 、．．．．．．．．．167
I11ustrations
Figu爬S：
2－1 Projected profi1e ofW－E direction of the northem part of the Abukuma Mountains．
2－2．Geomorphic map of the southem pa■t of Chubu district with specia1reference
to the distribution of the standa工d surface．
2・3．Profi1es ofNW－SE direction of the Mikawa High1and．
2・4－Topographical map of the typical erosion surfaces in Chugoku district，
southwestem Japan．
2・5．
2・6．
2・7．
2－8．
2－g，
2－10
2－11
2－12
2－13
2－14
2・15．
3・1．
3－2．
3・3．
3－4．
3－5．
3－6．
3・7．
3－8．
3－91
3－10．
3・11
3－123－13．
Distribution of the Kita・matsuura basa1ts and the cong1omerates and heights of the
basa1p1ains of the basa1ts．
Geologica1map of Teshio area．
Geologic pron1e of Teshio area．
Geo1ogica1map of Boso area．
Geo1ogic profi1e of Boso area．
Succession ofthe Boso Peninsu1a and its po1arity epoch．
Diagrammatic profile of Osaka Brasin．
Stratigraphic section of Kanto Basin．＿＿＿、＿．．
Pa1eomagnetic and paleontologica1chrono1ogy of Kazusa Group．
Corre1ation of paleomagnetic chIono1ogy，biostratigraphy and climatic chajlges
ofOsaka Group．
Profi1e ofNobi tilting b1ock．
Gipfe1nur map ofthe Kiso River va11ey．
Diagエam shoMng that Atera fau1t cuts seven steps ofriver terraces at Sakashjta．
Strike－s1ip fau1t system in centra1Japan．
Mobara，Geo1ogica1Maps of the Oi1and Gas Fie1d ofJapan．
Distribution of the fissure zones of probab1e fau1t origin or these which are
unable to be atnibuted to1andshde or the simp1e effect of gravity．
Distribution of mtic1ina1axes of Quatemary fo1ds in Japan，with1oca1ities of
Figures3－7，8，and9．
Restored contour map of the fo1ded river temces and their cross sections
inN09ataarea，centra1Japan．
Pronles of the terrace surface（mjdd1e），section of the geologic structure（1ower），
and the present vertical movements of1954＿1964（upper）in Funagata，northwest of
Sendai，northern Japan．
Restored contour map of the fo1ded coastal terraces and the cross section
in Nemuro area，eastem Hokkaido．
Thickness contoures of the Neogene md Pleistocene formation in Japan．
Re1ation between change of gradient or change of wave height and wavelength of
Quatemary fo1d in Japan．
Distribution of the rate（G／T）of Quatemary folding in Japan．
Distribution of direction of maximum compressive stress disc1osed by foca1
mechanism ofvery shallow earthquakes during the period from1927to1966、
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一5
3－14．
5・1．
5・2．
5・3．
5－4．
5・5．
5－6．
5・7．
5・8．
5・9．
5・10
5・11
5・12
5・13
5－14．
5・15．
5－16．
5・17．
5・18．
5－19．
5－20．
5・21．
5－22．
Distdbution of direction of maximum compressive stress estimated from active
strike－s1ip faults．
Major topography of Japan and its envi正ons・
Map ofJapan showing is1and－arc zona1ity．
Distribution ofCenozoic formations in Japan，with divisions ofNeogene provinces．
Vertical disp1acement since the Miocene．
Vertical disp1acement during the Quatemary．
Vertica1disp1acement during the Neogene．
Degree of deformation since the Miocene．
Degree offo1ding during the Quatemary．
Degree of deformation during the Neogene．
Re1ief at the present．
Re1ief at the end of the Tertiary．
Di．thb．ti。。。f。。1。。。。d・。・。gyby…thq・・k・・i・th・㎞・t・・i・p・・i・d（0・5。・m・・h・・）・
Distribution of released energy by earthqu虹kes
in the historic pehod（1。一meshes）．．＿＿．．．．．＿．．．．．．。＿＿＿＿＿＿．．．＿＿＿＿＿＿．．・Facing page
DistHbution of densities of fau1ts（1σ一meshes）．＿．＿＿．＿＿．＿＿＿＿＿＿．。＿。。、＿＿ “
Distribution of densities of fo1ds（1㍉meshes）． ……＿．＿＿一・＿……．……・・．．・＿＿＿ ”
Distdbution of max㎞um amounts ofup1ift．（1o－meshes）1＿＿＿．＿、＿、．。＿＿＿ ・・
Dist正ibution of ma対mum amounts of subsiden㏄（1㌧meshes）．．、．．、．．．．．．．．．．．．．．．． ”
Distribution of gradients（1o－meshes）．
Distribution of correction maximum subsidence amounts（1。一meshes）．＿、＿＿ ・・
Disthbution of comection gradients（1。一meshes）．。＿＿＿＿＿．．．＿．。＿＿、＿＿．＿＿ “
Gradients of Quatema取vertica1displacement．
Quatemary tectonic divisions of Japan．
Tab1es：
2－1． Heights of the erosion surfaces in the southwestem area of Chubu district．
2・2．Rate of cursta1movements in the Kanto Tectonic Basin since upPer Miocene．
3・1． Quatemary fo1ding areas．
5－1．Distribution of f正equencies of ma駅itudes of re1eased energy in the historic period
（from Fig．5－12）．
5－2． Distribution of frequencies of the densities of fau1ts and fo1ds c1assified
by the magnitude of released energy by earthquakes．
5－3．Distribution of frequencies of maximum upheava1quantities，maximum
subsidence amounts and gradients c1assified by the ma即itude of released
energy by earthquakes．
5－4．C1assi自cation ofthe Quatemary tectonic divisions of the Jap2mese Is1ands．
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1，111tr04uctiOn
The Japanese Is1ands be1ong to the circum・Pacific orogenic zone and have experienced severe
tectonic movements since the begiming of the Miocene Epoch，especia11y during the Quatemary
Period．The mode and intensity of the Quatemary tectonic movement have recent1y been e1ucidated，
but not yet been compi1ed as a who1e．0n the othe正hand，some of Quatemary tectonic movements
have been revea1ed to show the mode simi1ar to that of the remarkab1e crusta1deformation associated
with great earthquakes in historica1and recent times in the same areas．This fact suggests that the
studies on Quatemary tectonic movement wi11be usefu1fo川s to detect the history ofseismic activity
and may contribute to the fundamenta1research on prediction ofearthquakes．
F正om this point of view，the ReseaTch Group for Quatemary Tectonic Map was organized in
1963，in order to compi1e Quatemary tectonic maps of Japan which consist ofdistribution maps of
vertica1disp1acement，fau1tings and fo1d㎞gs in the Quatemary．The nna1goa1of the Research Group
is to compi1e maps of these kinds for different terms of103，104，105，and106years in the order and
to ana1yse the historica1processes and their regiona1characteristics of tectonic movement throughout
the Quatemary by comparing these maps．1t wi11be a1so interesting to find the re1ationships between
recent seismic activities and Quatemary tectonic movement and between the characters of tectonic
activities of the Quatemary and pre・Quatemary．
First of a11，the Research Group tried to comp1ete the distribution maps for the who1e
Quatemary．The first report with the preliminary tectonic maps was presented in1964to the
Nationa』Symposium for CRCM and was pub1ished in the Jouma1of Geodetic Society of Japan，Vol．
10．1965．These maps have been revised and supp1emented by recent1y obtained data．The second
report was presented to the7th Intemational Congress of the Intemational Union for Quatemary
Research in1965and was pub1ished in Quatemaria，Vol．8．1966．The Quatemary tectonic maps
pub1ished by the Nationa1Research Center for Disaster Prevention in1969consist of six sheets and
are considerab1y revised and supp1emented as compared with the former two reports．The present
report is the final for the whole Quatemary and is attached to the maps of1969，
Among these six sheets，the“Gipfemur”of Japan was former1y prepared by Dr．Toshi0
0kayama，Professor of MeOi University，but has not yet been pub1ished in a complete form．The
“Gipfe1f1ur”wi11be usefu1for comparing the magnitude and mode ofQuatemary tectonic movement
with the present1andforms of the Japanese Is1ands．We thank Dr．T．0kayama for his kindness on this
OCCaSiOn．
2．Quaten1趾y verticai disp1acement
Amounts of vertica1displacement for the whole Quatemary were estimated by geomorpho1o－
gical and geo1ogica1methods separate1y（Maps Nos．1and2）．Then，a synthesized map of vertical
disp1acement（Map No．3）was compi1ed from these two maps，comparing and examining every
amount in them．
2．1，Amomnts of vertica1displacement geomo叩ho1ogica皿y estimated
2．1．1．Method
Erosion surfaces，which are inferred as formed in the1ate P1iocene or early P1eistocene，are
distributed at different a1titudes in various regions of Japan，though most of them are genem11y
scattered．As it is considered that they were origina11y formed at1eve1s not very high above sea1eve1，
their present a1titudes above sea1eve1approximate1y represent the net amounts of vertical
disp1acement since the beginning of Quatemary，Strictly speaking，a1titudes above sea1evel at which
the erosion surfaces were initia11y formed should be subtracted from the present a1titudes to obtain
exact amounts of vertical disp1acement，but those can hard1y be estimated without any assumption．
Moreover，those must have been probab1y not so large，because extensivさ1y distributed erosion
surfaces with1ow re1ief are presumed to have been formed by rivers of which the gradients were not
so high．
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There are sevem1regions in Japan where the geomorphic deve1opment has been intensively
studied and the ages of erosion surfaces have been st1atigraphically determined」n these regions，
erosion suTfaces formed in the1ate Pliocene or ear1y Pleistocene were extracted so as to estimate
Quatemaw vertical disp1acement．Then，erosion surfaces corre1ated with these were su㏄essive－y
traced in their surrounding regions，using topographical and geologica1maps，together with the
“Gipfelf1ur”．In the process of tracing the simu1taneous1y formed erosion surfaces from one region to
another，it was examined in every we11－known region，whether or not the erosion surfaces had been
comct1y traced from one to another．It can not always be expected that erosion surfaces were
formed in the late P1iocene or ear1y Pleistocene and have been preserved unti1the present in every
region of Japan．From this reason，erosion surfaces formed in ages nearer to the above－mentioned
were used in some regions for estimating the amounts of Quatemary vertica1displacement・For
examp1e，erosion surfaces extensively beve11ing the upper Miocene formations were considered t0
have been formed in the period from1ate Pliocene to ear1y P1eistocene，because the extensive erosion
surfaces must have been completed in a considerab1y long dumtion of geo1ogica1time．Amounts of
vertica1disp1acement estimated by this method，therefore，aエe not exact1y for the Quatemary，but for
a term of〃x106years，〃being a certain number from one to two or three・Moreover，they can be
obtained on1y in up1ifted regions，because in remarkab1y subsiding regions the erosion surfaces have
presumably been buried under younger formations－
Heights of these erosion surfaces were read at about four points in each quadrang1e of
topographical map on a sca1e of1：50，000，and then the heights were p1otted in a map of Japan on a
sca1e of1：2，O00，000．1sobases in the Map No．1we正e drawn at interva1s of100or200meters based
on these heights．
2．1．2．Examp1es
a． τ0乃0κ〃Dゴ∫炉ゴCf
Erosion surfaces are extended on the outer side of the arc of Northeast Japan where the
Kitakami and Abukuma Mountains are located．
（i）肋θK肋肋洲〃oω舳α肋∫are main1y composed of the intense1y fo1ded Palaeozoic and Mesozoic
formations together with plutonic and metamorphic comp1exes．The erosion surfaces of the
Mountains are c1assified into three leve1s．The upper surfaces are1000to1200m high above sea1evel
and are presemed as f1at－topped ridges in the centra1part of the Mountains．The midd1e surfaces are
extensivelydistributedaroundtheuppersurfaces，andtheirheightsare800to900mhighabovesea1eve1．A1ong the ma∫gin of the Mountains，the1ower surfaces are distributed at the heights of500t0
600m，beve11ing the midd1e oT lower Pliocene in some places．As the middle P1eistocene marine
termces aTe developed a1ong the eastem side of the Mountains劃t an altitude of about300m，the
lower surfaces are presumed to have been formed at the end of P1iocene or the begiming of
P1eistocene．There is no evidence of marine invasion into the main part of the Mountains throughout
the younger Tertiary period．Any evidence of marked inflow of coarse c1astic materials into the
Miocene and P1iocene deposits adjacent to the Mountains is not recognized・Consequent1y，it is likely
that both the altitude and re1ief of the Kitakami Mountains remained very low during the TeTtiary
period（Chinzei，1966）．Since a tendency of increasing grain diameters can be recognized in the last
stage of the Pliocene deposition，the upheava1of the Kitakami Mountains is presumed to have taken
place main1y during the Quatemary．
（ii）肋ελ肋肋㎜α〃o〃〃α肋∫are main1y composed of granitic rocks w㎞ch intruded most1y in the
Mesozoic．The Mountains border on the Paci丘c coast by a steep scarp（Futaba fau1t scarp）ruming
from north to south with re1ative heights of more than400m，and seem to be inc1ined westwards．
Erosionsurfacesarewide1ydeve1opedata1titudes400to600mhighabovesealevelinthenorthem
ha1fof the Mountains．
Iso1ated f1at－topped peaks stand out on the erosion surfaces．Their heights range fエom800to1000m
above sea1eve1．Some of these peaks in the northem paTt of the Mountains are standing in areas
8一
consisting ofthe midd1e Miocenevolcanicrocks．Erosion surfaceswithlowerrelief1essthan50mare
recognized at six levels in the northwestem part of the Abukuma Mountains；name1y the Tokiwa，
Funehiki，Kumagami，Miharu，Upper Moki and Lower Moki erosion surfaces in a descending order
（Koike，1969；see Fig．2－1）．These erosion surfaces，successively stepping down westwards by30to60
m，extend from the south to the north like piedmont bench1ands．They were formed on the westem
back s1ope of the Abukuma ti1ted block by intermittent upheaval accompanying westward tilting．Six
levels of erosion surfaces，except the Miharu surface，mainly extend in areas consisting of deeply
weathered older granodiorite，Soon after the lower Moki erosion surfaces were formed，the Shirakawa
dacitic welded－tuffsΩowed and part1y covered the erosion surfaces lower than the Kumagami surface，
The eruption age of the Shirakawa dacitic we1ded・tuffs is not certain1y known，but it is estimated to
be the1刮test P1iocene or early Pleistocene．The lower P1iocene deposits w㎞ch are distributed a1ong
the eastem foot of the Futaba fau1t scarp were deformed by the activity of the Futaba fau1t，As the
E
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一9
above－mentioned intermittent upheava1accompanying westward ti1ting of the Mountains is estimated
to have a re1ation to the activity of the Futaba fau1t，the upheava1of the Abukuma Mountains is
presumed to have taken p1ace majn1y during the Quatemary．
（iii） In Uetsu area，e正osion surfaces are recognized at four1eve1s，though most ofthem are genemlly
scattered．Thisエegion is1ocated in the Green－Tuff r噌on，a young mobi1e region which has been
deve1oped since the begiming of the Miocene．As the boundaries of erosion surfaces are intricated，
they are considered to be formed in different ages．The highest erosion surfaces are main1y
f1at－toppedridgesata1titudesof1000to1200mabovesea1eve1andaredistributedinareascomposed of pre・Tertiary basements and1ower Miocene deposits．The second erosion surfaces
beve11ingthefo1dedmidd1eMiocenearedistributedinp1acesataltitudesof600to800mabovesea
1eve1．In Southwest Hokkaido，the second surfaces beve1the lower P1iocene in some places．Lower
third and forth erosion surfaces are distributed main1y a1ong the present va11eys and in the basins．
Their altitudes are in genera1lower than300m above sea leve1，After the deposition of midd1e or
upper P1iocene，many basins on the imer side ofNortheast Japanare formedbydifferentia1vertica1
movements，and1acustrine formations of the1ower P1eistocene were deposited in a㏄ordance with the
subsidence of the basins（Naito，1963．1970；Nakagawa，et al．，1971）．Then，lower erosion surfaces
were formed by beve11ing the P1iocene and1ower P1eistocene．It is，therefore，inferred that the
disp1acement of the second erosion surfaces occurTed after the1ate P1iocene，probab1y during the
Quatemary．
b．C乃αわ〃1）応〃た・f
（i）αo〃〃〃〃凶∫肋αnear the southem end of the inner side ofNortheast Japan has experienced active
crusta1movements in the Quatemary．After the deposition of marine upper P1iocene，the marine and
Ωuvial deposits of P1io－Pleistocene or1ower P1eistocene，Uonuma Group，were thickly a㏄umulated
in accordance with the subsidence of this region．This region was not yet differentiated into basins
and hi11s in the first half of the Uonuma stage，when the Echigo Mountains located to the east
supp1ied sediments to form an extensive depositiona1p1ain」n the1atter ha1f of the Uonuma stage，
this region was divided into basins and hi11s and was tumed into upheava1（Naito，1965）．It is
therefore inferred that erosion surfaces of the Echigo Mountains and depositional surfaces of the
Uonuma Hil1s were displaced mainly after the ear1y P1eistocene．The a1titudes of erosion surfaces of
the Echigo Mountains are900to1200m above sea1evel．
（ii）”or肋θ閉ρα〃o∫一Mα8α〃o〃ε作α〃θ．In the northem part ofNagano Prefecture，erosion surfaces
arerecognizedatfourlevelsandaredistributedataltitudesof2000m，1700m，1400m，and1000＿
800mabovesealevelinadescendingorder（Kobayashi，1953）．Theerosionsurfaces1000to800mhigh are refened to as the“0mine erosion surfaces”。The Omine erosion surfaces are distributed
main1y in areas composed of the Tertiary rocks，and peaks standing on the erosion surfaces，are
considered to be H包rt1ing．F1uviati1e bou1ders are found in some p1aces of the Omine erosion surfaces．
These boulders are composed m虹n1y of granitic rocks，some of them being three meters in diameter．
It is therefore considered that the boulders were derived fmm the Hida Ranges1ocated to the west of
the northem Fossa Magna and were deposited at the1atest stage of the formation of the Omine
erosion surfaces．The Hida Ranges border a steep scarp（Hida fau1t scarp）running from north to south
withare1ativehei餉tofabout2000m（Tsujimum，1926）．IntheeastempartoftheHidaRanges・
erosion surfacesare recognizedata1titudesof2700m，2400m，2200＿2000m，and1800＿1600m
abovesealevel（KobayashiandHirabayashi，1955）．Theerosionsurfaces1800－1600mhighontheHida Ranges are considered to be corre1ative with the Omine erosion surfaces．The deposition of
boulders on the Omine erosion surfaces indicates the rejuvenation of the upper drainage of the rivers
and an increase in stream gradient，and therefore it might suggest the upheava1of the Hida Ranges．
The Omine erosion surfaces beve1the Plio・Pleistocene or1ower P1eistocene marine formations．The
lava nows which are corre1ated to the above－mentioned marine formations are most1y reversed in
magnetic direction，suggesting that they are referab1e to the Matsuyama reversed epoch in age
－10一
（Momose，1963；Research Group on the Quatemary ofJapan，1969）．It is therefore inferred that the
Omine erosion surfaces were formed during the early to midd1e Pleistocene and that the rapid
upheava1of the Hida Ranges occurred after the ear1y P1eistocene．
（iii）肋ε〃肋wα〃助伽〃composed of main1y臣anitic rocks o㏄upies the southeastem part ofthe
area shown in Fig．2・2．This hi如and is bordered on the northwest by the straight steep scarp，
“Byobusan fault scarp”，w㎞ch is mnning southwestward from the Em Mountains．This1ow－re1ief
hiε阯and genera11y decreases its a1titude southwestward，and also tow虹ds the Y出agi Rjver which
flows through the centra1p町t of this high1and．
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Geomorphic map of the southem part of the Chubu district（Kaizukaθfα1．，1964）
1：Bedrock mountains rising above the depositional surface of the
Seto Group in the area a1ong the Rivers Kiso and Toki．
2＝Distribution of the Seto Group，containing the area covered with
the younger deposits．
3＝Contours of the Gipfe1f1ur．In the自rea a1ong the Rivers Kiso and
Yahagi，contours are drawn intheparthigherthan700m，andin
otherareasinthe parthigherthan300m．4：ContouIs of the depositiona1surface of the Seto Group．
5：Bedrock contours under the Seto Group．
6：Fault scarps．Most of them have been dislocated after the
deposition ofthe Seto Group．
11一
Erosion surfaces of various leve1s are developed in this high1and．A1though the higher two
erosionsurfaces，1100＿1000mand900＿700mhighabovesea1eve1，showonlytheirre1ative1y1hnited distTibution near the top of the mountains，an erosion surface1ower than600m is very
extensive1y deve1oped．This surface is caned the Mikawa erosion surface and is subdMded into two
leve1s，the Mikawa higher（600＿400m）and the Mikawa1owe正（300＿100m）surfaces，Figs．2－2and
2・3 show the horizontal and vertica1re1ations between the Mikawa lower surface and the
P1io－P1eistocene Seto Group which is widely distributed in this area．It can be seen from these figures
that the Mikawa lower surface is continuous to the basa1surface ofthe Seto Group which shows a1so
the low－re1ief topography－Moreover，the Mikawa1ower surface extends northward，bevel1ing the
midd1e Miocene Mizunami Group．A㏄ording1y，it is most probab1e that this surface was fonmed in
the ear1y P1iocene（Otaαα1．，1963）．Therefore，the heights of this surface were adopted to estimate
the Quatemary vertical disp1acement．
NW SE
800S
＾ ・汕’“・…
400
11’一1’’ 皿㎜0SC
＾
20KM lOO B
Fig．2－3．Profi1e of NW－SE direction of the Mikawa High1and（0taθfα1．，
1963）．Dotted zone represents the Mikawa1ow erosion surface an
the depositiona1surface of the Seto Group．The former has been
dis1ocated a1ong the Asuke fau1t．Location of the cross1ine is
shown in Fig．2－2．
The Seto Group is subdivided into two formations representing the different depositiona1
environments and ages．The1ower formation of it consists ofvery Hne・grained sediments derived from
the weathered materia1s of granitic rocks．On the other hand，in the upper formation which over1ies
the1ower unconformably，coarse sand and grave1s are domimnt．These facts suggest that in the early
stage of the deposition of the Seto Group，the Mikawa High1and was very1ow in re1ief，representing
the Mikawa lower surfaces，and was the source area of fine－grained sediments，and that afterwards the
Mikawa High1and was uplifted to1ie intensively dissected and to supp1y a great amount of coarse
sediments．In comection with the uplift of the Mikawa Highland area，the Yahagi River basin has
been down－warped since the P1iocene，with an axis ofNE－SW trend a㏄ompanying the faults with the
same direction along its both sides．
The mountainland located northwestward from the Byobusan fau1t scarp is divided into three
mountains：肋θ〃θ〃in the northeast，〃κハ〃α舳㎜o〃in the middle and肋θKθ〃8アo in the
southwest，by the Atera and Akagawa fau1t scarps which run with NW－SE trend（Fig．2－2）．In these
mountains，the higher and lower erosion surfaces and the depositiona1surface of the P1io－Pleistocene
Seto G正oup are developed in the descending order（Kiso，1963；Kaizukaαα1．，1963；Kaizukaθfα五，
1964）、The1ower surfaces in these mountain1ands are continuous to the basa1p1ane of the Set0
Group and beve1the Miocene series．A㏄ordin創y，it is possible that the lower surfaces were formed in
the ear1y Pliocene and are correlated with the Mikawa1ower surface in the Mikawa High1and．
Although there is no evidence to show the age of the formation of the higher erosion surface，
probably it was formed in the pre－Miocene，judging from the re1ation between the distribution of this
surface and the Miocene series．
一12
Therefore，the heights of the1ower erosion surface were adopted to draw the Quatemary
tectonic map．In addition，the deposition surface of the Seto Group is a1so used in this area，
Consequent1y，the geomorphic surfaces which are used for the estimation of Quatemary vertica1
disp1acement in this area were formed in a fairly longer term．
The hei創1ts of these geomorphic surfaces are represented in Table2－1．The difference of the
hei出ts in the same surface among the three mountains has been caused by the differentia1up1ift with
the faults shown in Fig．2－2．Some of these fau1ts contributing to the differentiation of the mountains
are sti11active．Especia11y，the Atera fau1t is a very typica1active fau1t dis1ocating the recent f1uvia1
terraCeS．
Tab1e2－1． Heights of the eIosion surfaces in the
southwestern area of the Chubu District
Mikawa High1and Atem Mts． Futatsumori Mts、 Ke㎎yo Mts．
UPPer su正face1000＿11OO m700－gOO m
1400＿1700m 800＿1000m 700＿800m
Lowcr surface（Mikawa su正face） 400＿600 m1OO＿300 m
900＿1200m 500＿700 m 100＿300m
C． Kゴ〃κゴDゴ∫f1プCf
In the inner zone of胞nki District，severa1mountains with N－S trend are distributed in para11el，
and among these mountains there are1ocated the basins such as Iga Basin and Nara Basin bordered
with fault scarps，In these mountains，remnants of former erosion surfaces are preserved in
accordance with summit Ievels，especia11y very widely in the Nunobiki Mountains situated in the east．
The age of the formation of erosion surfaces was discussed by Nakano（1944），analysing the re1ation
between the erosion surface and the Cenozoic strata．
（i）The erosion surface on the top of肋θ〃〃τoわ榊〃o〃舳α肋∫is at altitudes ranging from600to700
m，and is intersecting the basal surface of the Miocene lsshi Group．Hence it can be said that this
surface was f（〕rmed in the post－Miocene．
（ii）In沽θγα㎜〃o〃助1舳d situated to the west ofthe Nunobiki Mountains beyond the Iga Basin，an
emsionsurfaceabout500mhighwaspossib1yformeda1sointhepost－Miocene，becauseitbeve1stheMi（〕cene strata．
（iii）On the top of肋θRo肋o〃o〃吻肋∫in the most westem part of Kinki District，the erosion
surfaceatana1titudeofabout800misdeve1oped．0nthefau1tstepborderingthesouthemsideofthe RokkoMountains，thereisanerosionsurface coveredwithathinsandandgrave1bedwhichisthe1owest member of the P1io・P1eistocene Osaka Group．Huzita（1962）regarded this basa1surface to be
corre1ative to the erosion surface on the top of the mountains and to have been formed during the
Miocene－P1iocene．This surface，therefore，is correlated with the erosion surfaces in the Yamato
HighlandandNunobikiMountains． The Miocene series in the imer zone of Kinki District generany show the zonal distribution
from east to west inc1uding the both areas of mountains and basins．On the other hand，the
distribution of the P1io－Pleistocene series is restricted to basin areas or coasta1areas．From the
above－mentioned facts and the distribution of erosion surfaces，historica1development of this area is
assumed as fol1ows．1n the ear1y Miocene the subsiding zone with E－W trend was formed，and the
subsequent transgression caused the deposition of Miocene marine strata in this zone and buried the
re1ief of the mountains．Then，in the工ate Miocene this zone was uplifted and the erosion surfaces
bevel1ing the Miocene series were extensively formed by subaeria1erosion．In the early Pliocene again
一13
the subsiding zone with E・W trend was formed to deposit the1acustrine sediments in inland areas・
Since then，this subsiding region has been up1ifted and differentiated into the mountains md basins，
a㏄ompanying the thrust fau1ts with N－S trend．
d． 0乃〃9oκ〃1）ゴ∫〃．たτ
Chugoku ditrict is one of the most typica1areas where the erosion surfaces with low re1ief
are extensive1y deve1oped（for example，see Fig．24）．This district is known as the a正ea where the
c・・ceptoftheupliftedpenep1・in，㎝thebasis・fthecyclictheo・yofe・osion，hasbe㎝apP1iedfo・
the first t㎞e in Japan（Koto，1908）．
The erosion surfaces of this district are c1assified into three levels，the Dogosan surface，the
Kibikogen surface and the Setouchi surface in the descending order（Nishimura，1963）．The Dogosan
surfaceispresewedonthetopsoftheChugokuMountainsabout1000mhigh．TheKibikogensurface ranging from400to600m high above sea1eve1is developed in the area sunounding the
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Dogosansurface，andespecia11yonitssouthside・TheSetouchisurface1essthan200m㎞ghis1ocatedto the south of the Kibikogen surface，facing the Seto In1and Sea．
In Chugoku district，the re1ation between the distributions of erosion surfaces and the
Cenozoic strata has been exp1ained as fonows．The Miocene series are distributed mainly in the area
of the Kibikogen surface，part1y invading a1ong the va11eys into the Dogosan surface．The upper limit
ofdistributionoftheMioceneseriesisabout800mhigh，higherthanthatoftheKibikogensurface．In the va1leys dissecting the Kibikogen surface，the lower Pleistocene series is formed．From the
above－mentioned facts，it is inferred as to the age of the erosion surfaces as fonows（0tuka，1937）．
The Dogosan surface was formed in the pre・Miocene，probab1y in post－Cretaceous age，and the
Kibik・g・・…f…i・th・Pli・・…，th・・th・S・t…hi…f…i・th・1・t・・tP1i・・・・・・・…1y
P1eistocene．To estimate Quatemary vertica1displacement in this area，the height of the Kibikogen
surface was used・The mode of the crustal movement of this dis打ict in the QuatemaW was of an
up－warping with a1ong axis ruming from east to west，a㏄ompanied by faults，especia11y on the
southern side．
e．K〃∫肋〃∫肋cf
The dissected1ava p1ateau extends in肋θ〃07肋wθ∫κ川ρσ1・f oアκノ〃曲〃．The surface of the
p1ateau gradua11y1owers from east to west．The Kunimi－y㎜a（777m high above sea leve1）is the
highest part㎞the eastem margin of the p1ateau．The thic㎞ess of the basalt lava isgenera11y about
300m，and the basalplane ofbasa1tsisgener汕yf1atandpara11e1withthe surfa㏄ofthe p1ateau．The
basement of the basa1t1ava is composed mainly of the fo1ded Miocene，and the cong1omerates part1y
over1ie the bas刈surfaces（Fig．2－5）．The o㏄urrence of the cong1omerates is not continuous and its
・ a二秒 ・簿萎婁婁婁婁嚢 ’！ 9／一’蓼、対ぐ＝・髪ギ151
1思沸1妙／瓜＼’
為、漸蓼榊ザ’榊・一・1ぶR1 烹
炉’ 瓢伽、。繊1…30。
・㌧ ． εσ｛㌔・広6削。嚢m 180120 N
。 十
㈱。1 0 2 4 6 810k．n ．’’2 （；；。5 一一狐 物3 ／ 6 ・150 ’1100
Fig．2－5．Distribution of the Kita－matsuum basalts and the cong1omerates and the
heights of the basa1p1ane of the b副sa1ts（Imaiαα五，1958）．
1：UpPer conglomerate．
2：Loweτcon創omerate．
3：The position of the outcrop with direct contact between the Tertiary
strata and the basa1t1ave f1ows．
41Distribution of the Kita－matsuuエa basa1ts．
5：Contour1ine showing the basa1p1ane of the basalts，
6＝Main fau1ts、
15
thic㎞ess varies from sever創decimeters to one meter．The創titude ofits distribution is a1so variab1e，
from460m high above sea1evel near the Kun㎞i－yama in the east to O m high in the west（Imaiααム，
1958）1As a resu1t of the p創aeomagnetic investigation，the basa1tic activities are considered to have
lasted for a1ong period，probab1y from the middle P1iocene to the P1eistocene（Kurasawa，1967）、1t is
infemd that the cong1omerates might have been deposited duhng or immediate1y a耐er the
formation of the f1at basa1p1ane of basa1ts，and therefore that the p1ane might have been formed in
the midd1e of the P1iocene．
f．Rψ肥〃oθ∫
Chinzei，K．（1966）：YoungerTertiarygeology oftheMabechi RiverVa11ey，Northeast Honshu，Japan・
．1．Fαc．8cゴ．σηル．τoκノo，Sec．H Vo1．16，pp．161＿208（加亙ηg〃3乃）。
Huzita，K．（1962）：Tectonic deve1opment of the median zone（Setouchi）of Southwest Japan，since
Miocene．、1．0εo∫c’．0∫ακαC〃γσηル、，Vo1．2，pp．l03＿144（肋E〃g1舳）．
Imai，I．，K．Sawamura and T．Yoshida（1958）：Imari，Geo1，Map of Japan，Sca1e in l150，000．lGθ〇五
8〃．∫αραη（加切αη鮒W舳亙榊∫んαわ舳α）．
Kaizuka et aL，（1963）：Geomorphology of Japan。λ∬・GθoムCo”泌・∫αρ舳・Tokyo（inノαραηθ∫θ）・
Kaizuka et a1．，（1964）：Geomorphic development of the drainage basins of the Kiso and the Yahagi，
Centra1Japan．0θo肌Rθリ．∫αραη，Vol．37，pp．89－102（肋∫αραηεκw舳亙ηg〃肋αb∫肋α）．
附so，T．（1963）：Geomorphic development of the Hida－Mino Highland，Centra1Japan．0θogr．伽ソ。
∫αραη，Vo1．36，pp．87＿109（肋∫αραηθJεw〃ん亙η8〃∫わαゐ∫卯αα）．
Kobayashi，K．（1953） Pleistocene erosion surfaces in the westem part ofthe“Fossa Magna”．0εog7－
Rθツ．．1αραη，Vo1．26，pp．291＿307（肋ノαραηε∫θwゴ肋亙ηg〃曲αわ∫卯αα）．
Kobayashi，K，and T．Hirabayashi（1955）：On the so－ca11ed“mountain boulder grave1”around
Matsumoto Basin．ノ．Gεo1．8oc．∫αραη，Vo1．61，pp．30＿47（肋∫αραηθ∫θw舳肋g伽んα加伽α）．
Koike，K．（1969）：Geomorphologica1deve1opment of the Abukuma Mountains and its surroundings，
Northeast Japan．∫oρα〃．∫Gθ〇五Gθog7．，Vol．40，PP，1－24（加Eηg〃∫乃）・
Koto，B．（1908）：Physiographic type ofChugoku．Rθρ、∫㎜ρ、E〃〃岬．1ηリーCo〃！〃一．63，PP・1－15（〃一
切αηε∫θ）．
Kurasawa，H．（1967）：Petrology of the Kita・matsuura basa1t in the northwest Kyushu，Southwest
Japan．Rθρ．No．217，0εoム8〃．∫αραη（肋万〃g1ゴ曲）．
Momose，K．（1963）：Studies on the variations of the earth’s ma馴etic行eld during Pliocene time。肋〃。
肋〃切．Rε∫、1η∫f．，Vo1，41，pp．487＿534（加亙ηg〃ψ）．
Naito，H．（1963）：Geomorphic deve1opment of the Takanosu Basin，Akita Pref．，Northeast Japan．
Gθogr．R〃．、1αραη，Vo1．36，PP．655－668（肋∫αραηωεw〃わEη8〃肋αわ∫〃αα）・
Naito，H．（1965）：Landforms around Tokamachi City，Niigata Pref．，＿Geomorphic deve1opment of
Uonuma District＿．0θogr．伽リ．∫αραη，Vo1．38，pp，613＿629（肋∫αραηθ∫θw舳肋g〃∫乃
αわ∫伽α）、
Naito，H．（1970）：Geomorphic deve1opment of the Hanawa Basin and the Odate Basin，Akita Pref・，
Northeast Japan．Gεo肌Rεリ．∫αραη，Vo1，43，pp．594＿606（肋∫αρ舳θ∫θw〃一Eηψ∫乃αわ∫肋α）．
Nakagawa，H．αα1．，（1971）：Quatemary crusta1㎞ovements in the Shinjo Basin，Northeastem Honshu，Japan．Co〃κ1伽’．Gθoム，Pα1．，τo1－oκ〃σ〃リ．，No．71，pp．13－29（肋。1αραηθ∫εw〃乃
亙η9舳肋∫舳α）．
Nakano，T．（1944）：The age of the erosion surface in Kinki District．0θog尺Rεひ．∫αραη，Vo1．20，pp．
12－33（1〃αραη㈹）．
Nishimura，K．（1963）：Chugoku Mountains as a staircase morpho1ogy．8cf一伽ρ．τo乃oκμσηル。，7th
Ser．（Geography），No．12，pp．1＿19（加亙ηg〃∫わ）．
0ta，Y．αα1．，（1963）：A geomorphologica1study of the Mikawa Highland and terraces of the
adjacent district．Gεo肌R〃．∫αρα〃，Vo1．36，PP．617－624（肋∫αραηθ∫θw〃一亙ηψ肋αわ∫〃αα）・
0tuka，Y．（1937）：General morpho1ogy of Chugoku Mountainland and its geo1ogical age．∫Gθogr。，
Vo1．49，pp．156＿162（肋∫αραηωθ）．
Research Group on the Quatemary of Japan（1969）：Quatemary system of Japan。〃o〃og尺！5，
舳・・．Gε・1．C・肋．∫αραη（肋切αηθ∫川舳E・91舳αわ舳α）．
Tsujimura，T．（1926）：Deve1opment of composite fault scarps．∫．Gθo1－8oc．τo灯o，Vo1．33，pp．
75＿90（加∫αραηθ∫ε）．
一16＿
2．2．Amounts of vertica1displacement geo1ogica11y estim汕ed
2．2．1．Method
Heig11t and depth or bounda1・y horizons between the marine Pliocene and Pleistocene
止brmations approximate1y represent the net amounts of vertica1displacement during the who1e
Quatemary．In this case，ωo，it is necessary to c（〕rrect these va1ues in order to estimate exact amounts
of Quatemary vertical displacement，because these boundary horizons must have been original1y
1ocated more or less deep be1ow sea1eve1，But it is hard1y possib1e，without any assumption，to
estimate the depth at which these formations were initially deposited．In the present work，therefore，
no correction was done to estimate the amounts of Quatemary vertica1disp1acement by a geo1ogical
111ethod，
1n uplifted al・e二1s，b（π1ndary h（〕riz〔）ns between the marine Pliocene and Pleistocene formations
・・・・…1ly一…t・d・b・・・…1…1・tp・・se・t，・・diti・…elyp・s・ib1・t・丘・ds・・hbo・・d・・yho・i・o・s
in sedimentary sl1㏄essjon from the P1iocene to the P1eistocene，because P1iocene fo㎜ations have
been generally demlded and have not been overlain by younger ones at most p1aces．From this reason，
11eig11ts（〕f the higl／est pointsofupperPliocenemarinefo㎜ationswere usedtoestimateapproximate
amounts of Quatemary vertical displacement．Strict1y speaking，as result of denudation these heights
do not represent heights of the origina1deposition surfaces of these formations，which are more
appropriate for the present work．The highest points of1ower Pleistocene formations were also
adopted for the same purp（）se in the present work．
Some convenient methods were used in areas where formations of the above－mentioned ages are
not distributed．That is，assuming that the rates of tectonic movement have been uniform since the
beginning oゴthe Pliocene－he height of“1ower”Pliocene formations is estimated at twice as1arge as，
and1hat of“middle”Pleistocene formation at one third as large as the amount of vertical
disp1acementゴ（〕r the who1e Quatemary，These amounts are shown in the Map No．2with special
symbo－s・The abs（〕lute ages of these formations and of the beginning of the Quatemary have not yet
definitely been determined，and it is problematical whether the above assumption is correct or not．
These estimations，therefore，were applied only to such cases as any other data cou1d not be obtained
『O『eXtenSiVC arCaS．
In subsiding areas，da－a oゴdeep drinings were used，because the said horizons are usuany
1oじHtcd11nder allし1viHl p1ains，b～1sin Ooors，coasta1plains，or submarine bottoms at present．There are，
however，only a Few areas where the said horizons have definite1y been determined．In other subsiding
areas，st）me coηvenient processes such as adopted in uplifted areas were app1ied．In these cases a1so，
nmounts or vertical disp－acement were not corrected by using the depths be1ow sea1eve1at which the
Pli（〕一Pl・i・t・・…ゴ・1’m・ti…h・di・iti・llyb…d・p・sit・d．
The upper Pliocene formations of Japan are shown in the conelation tab1e of the Neogene
「ormations in t11e“Geologic Deve1opments of the Japanese lslands”（1965）．Ages of loca11y
distribu1ed Pliocene r（〕rmations which are not contained in this table were determined on the basis of
their geomorph〔〕k〕gica1and stratig11aphical relations to the formations contained in the tab1e．
ThereF（〕rc－hcゴ〔〕rmations adopted as the upper P1iocene in this work may not always be of the same
agc■〕ut must have becn deposited〔luring a short period from the Pliocene to the Pleistocene．
D汕い〕ゴhcight o－1dcpth of these formations were obtained from geologica1maps of various
sca1es pl1blishcd by the Geologica1Survey ofJapan，geo1ogica1maps ofeach prefecture，and scientific
papers and reports・In principle，amounts of Quaternary vertica1disp1acement were estimated in each
quadrangle of topographical map of l：50，000at one point，wheTe the said formations are1ocated
highcsHn uplifted areas and k〕west in subsiding areas．Then，these amounts were p1otted in a
map oゴ』卯an on a scale of112，000，000．1sobasesin theMapNo．2were drawnatinterva1sof100or
200η1eters by the interpolation lneth（）d，
2．2．2．Examp1es
a．σρ々伽11α1でα．，．
一一17
（i）τθ∫〃o〃θα（Figs．2－6and2・7）
Upper P1iocene lying in this area is Sarapetsu formation corresponding to Setam formation．
Sarapetsu formation has the thickness of200＿350m，composed of altemating strata and considered
as formation of1agoon origin．A㏄ordingly，the deve1opment of this formation can be assumed to
represent the1eve1s which were extremely near to the sea1evel of those days－This formation，together
withYuchiformation（200mthick）andKoetoiformation（300mthick）（bothbeingofmarineorigin and bel㎝gi㎎to㎞e Lower Pliocene）which c㎝fomab1y1ie under Sarapetsu fomation，
composes the h皿1s of heights less than200m in the who1e neighborhood of Teshio，showing gent1e
nexure．A㏄ording1y，it can be said that the heights of hi11s in this area we11ref1ect the approximate
shapesofQuatemaWgroundup1iftingofthisarea．
べゐ
X
〕
’
lOkm
舳1l1
伽1 ’
1
ll．
I11
．1鰍
．
11，
亭ト1、
Tし室
■
簑，．‘
毒’・：く、
I’
｝
う1■
，’
、
．・苫
珊1鰍
鱒11
Y
ロ ロ 皿 囲 蟹 圏 ㎜＾llwium Dilwium Sombetsu F．Yuchi F． K06toiト． W副kkami F．P爬・Wakkmi F－
UP．Pli0－ Low．P1io． Low，Plio． Up．Mio．
Fig．2－6．Geo1ogical map of Teshio area一
50♂
11」一・・。、鱗鞍、1繍1，1．．、1甘．．．r
Fig．2・7． Geo1ogic profi1e of Teshio area．
18
In the eastem part of Horonobe area a1ong the River Teshio，the axis of antic1ine extends
north・south in the Miocene fomation．Having gone across thisa対s，㎝theeastsidethereisseen the
distribution of Sarapetsu fomation，centeri㎎around Toikanbetsu．Therefore，the sedimentary
domain of Sarapetsu formation can be considered to have extended across the Miocene antic1im1axis，
and the distributi㎝of Sarapetsu fomation is estimated to have deve1oped over this antic1in杣a対s．
But the thic㎞ess of Sarapetsu fomation thus estimated，and those of the fomati㎝Yuchi and
Koetoi a1so are not c1ear1y㎞own．There may be some possibi1ity that in the case where these
formations were thin over the antic1ina1axis，the height of Sarapetsu formation over the a対a1part
only slightly surpassed the present heights of the Miocene formations．However，as these formations
are wide1y distributed on the both sides of antic1ina1axis in t㎞s area，it would be aうpropriate to
consider that these formations were deposited over the antic1ina1axis a1so，though being made
somewhat thinner．From such consideration，the ma対mum amount of upheava1is estimated to be
over400m．（ii）30∫0ακα
The Boso Peninsula is one of the standard regions in Japan for the discussion of the boundary
between the Tertiary and the Quatemary．In the Boso Penin．su1a，there are deve1oped marine deposits
of the period fmm Miocene to Pleistocene，severa1thousand meters thick，almost making one
continuous series，and tilting toward the north，A sequence of stmta a1ong the River Y6r6
streaming northward in the central part of the peninsu1a is regarded as a stratigraphic standard，and it
is shown in Figs．2－8，2－9and2－10．
It is supposed that in the midd1e part of Umegase formation there1ies the Plio－Pleistocene
boundary．Thjs boundary was presumed on the basis of the study of Asano（1957）on
planktonic foraminifera．A㏄ording to him，at a position upper than the midd1e part of Umegase
formation，there became conspicuous the existence of a co1d sea sp㏄iesαoわなθ肋αあoκα〃∫，and this
was regarded as what indicates the“耐st cold c1imate”and as the commencement of Quatemary，This
concept was afterwards supported by the study on p1ant fossi1of Kokawa（1969）and a1so by the
pa1aeogeomagnetic study of Nakagawaαα五（1969）．Umegase fo㎜ation is an砒emation ofstrata
rich in sand with a pyrop1astic key bed U6．The sedimentaW formation of U6horizon，which is
designated as P1io・Pleistocene boundary，has the mol1uscan assemb1age which indicates the
sedimentary environment oflower neritic sea zone－h釦f abyssa1zone genera11y under the influence of
ocean waters．We may be able to say that the U6horizon was deposited at origina1depths of300－
500mformostofthepeninsu1aandatorigina1depthsof200＿300mfo正thewestempartofthepeninsu1a．
In the westempartofthepeninsu1athemaximumva1ue oftheheightofoutcrop ofU6hohzon
is200m，and if its depositiona1depth be300m，the total quantity of upheava1in this case wi11be
500m．However，U6horizon must have its extension on the southem side of its surface outcrop
before denudation．If the genera1slope of10o N in the vicinity of this p1ace were reverse1y extended，
the upheaval amount on the sou砒em side ought to have a pretty1arge va1ue．Presuning from the
circumstances that the genera1dip on the southem side becomes gradua11y steeper and shows va1ues
of more than6ゴN beneath Kurotaki unconformity（base of Takeoka tufo and that these beds
inc1uding U6horizon are rather oceanic so that any1and area is not conceivable at a distance very
cIose to them，the maximum amount of upheaval wou1d be not1ess than500m even if reduction of
depositiona1dep血shou1dbedone．
Further，Mt．Kanosan on the northem side of the area where U6horizon is deve1oped has a
height of350m above sea1eve1，and this va1ue is the max㎞um height of Ich司uku sand bed which
immediately over1ies the U6horizon．As Ich珂uku sand bed is砒e sediment㎞upper neritic sea zone
or de1ta，its sed㎞entary depth is considered to be nearly O m．A㏄ording1y，the upheava1amount of
Ich功ukusandbedcanbesaidtohavereached300mat1east．
Therefore，it is not an overestimation to consider the upheava1amount ofthe lower Pleistocene
一19
to be more than500m．And the beds of the Boso Peninsu1a which are deve1oped in east－west
direction，inc1uding U6horizon，can be regarded as those that show the pattem of upheavai
comesponding to the geo1ogic structure of northward s1oping．
As the development of this structure was formed by gradua1transposition of the sedimentary
basin，it cannot be expected that a formation，e．g．Umegase formation，wi11maintain its bed thickness
for a1ong distance on the southern side of its present surface distribution．Therefore，the upheava1
amount of U6horizon，though it evident1y surpasses500m，camot maintain the va1ue in the
southward direction．
A
■．§ll
．11鷲1
■
． 1 ‘ ． ． 1 ．
■ ■ ■ 一
顯、・．細・
5km
口＝1鴛
口 竃Sanuki F－ lchijuku F．
Nag刮k顯moF。
皿1wasaka F，
Awagumド．
田饒鮒．
園Sak纈h副一aト．
丁齪k皿mizoト．
繍．．’lI
1．1！
．
㎜ 。
Tomiya F．
Tak00ka F、
1・
Fig．2－8． Geo1o虫ca1map of Boso area．
：：l／＾
lll＋一・・一
Fig．2－9．
い・’’二．1’ ．、ス．1、。・言一繕壮’一雫、T、。、
Geo1ogic profi1e of Boso area．
一20
皇］←
FORMATlON ＞ 己三
ControlBoso← ｝一＝＝9山
westemBoso竺U≡～＜oΣ〉一宍くδ09L」 ≦9
爽畠畠
Kioroshiト． ooam11waashi一 ■一
SemataF． ξC畠目
ω仁
YabuF．
8 JlzodoPε SanukiF． KasamoriF．
U〇一串＜
吻■一
O NagahamaF、 Manano・口」 Chomn・
KakinokidaiF．
二…；）⊃竺 】o 国Z
lchijukuF．
K（）kumotoト’0rmatiOn
＜o；一＜oo
訂＞坐）コo
UmegaSe ←＞
マ〃〆 ト0rmatiOn一一U6 く］
；生
Otadai
一 易＜ε⊇；）＜生
ooTak1mlizoF． FOrmatiOn Z
o←口
o⊆①O
（曽竃こ雪睾
．2 弗匡
TomiyaF．Kiwada 一Formation ＜
＾ 妻い） 生
◎
z
（ ＞
TakaokaF． KurotakiF．
o ’） 竺
AnnoF． AnnoFormation 一
＜（ 量じ坐
ω⊆
Kiyosumi oFormation z
ωo
．9
妻
AmatsuFormatio11
」…・
Fig．2－10． Su㏄ession of the geo1ogica1formations and po1arity
epochin the Boso Peninsu1a．
一21
In the vicinities of the southeast end ofSouth Kanto District，the above－mentioned tendency of
“south・high”simi1ar to the Boso Peninsula is recognized in the Miura Peninsula and Oiso Hms also，
and this is cal1ed Tanzawa・Mineoka upheaval belt．This crusta1movement continued from the1ate
Miocene to the Quatemaワ．
（iii）肋Ro肋o〃o〃舳肋∫（Fig．2－11）
The Rokko Mountains situated west of Osaka City has the ma対mum height of932m，and
divides the basi∫1s of Osaka md Harima which are deve1oped on ule east and west sides of the
mountains．In the both basins仇ere are deve1oped beds of Osaka Group which is plio－P1eistocene
series，and especia11y the outcrops from the east foot of Mt．Rokko as far as Senriyama Hi11s，Osaka
Preiecture，give the standard stratigraphy ofthe Osaka Group．
OSAK｛
北一〇。d1， H1宮h町泓1r帖〔e ＋ 一〇m〔o
＾lluw1肌1了f田仁～ ・ M撒、
。・。。 一ミしI唖堕；τ；川；ニニ■I、三．
十∴∵∴1・、、蛍汁三二
KAW＾〔’1H － lOOO n1
L二胤、
一＝．一二二一ニニニ＝■■ Io〔k、
・・一キt三：l1二凸三1二．．、ぐ… 十
Fig．2－11． Diagramm副tic profile of Osaka Basin．
（Modified from the diagram by Itihara，1966）．
The Osaka Group developed in the area of Senriyama Hi11s is，a㏄ording to Itihara（1961）．
agroupofbedswhichcanbedividedintotwoparts，upperξmdlower，theupperpartbeing80mthick，the1ower200m，md respective1y composed of altemation of strata of sand，mud and grave1of
brackish water sediment and of freshwater sediment．In the upper part there are interposed beds of
marine mudstone of Ma2－Ma8，and in the lower those of Ma0－Ma1．
A㏄ording to the palaeomagnetic stratigraphic study of Ishida，Maenaka and Yokoyama（1969），
the horizon of01duvai event to be regarded as the Plio・P1eistocene boundary lies under Ma O and near
the Kono tuff，name1y in the middle of the1ower part ofOsaka Group．
Huzita and Kasama（1965）indicate，in their genera1view of the structura1deve1opment of
Cenozoic strata inc1uding Rokko Mountains and Osaka Basin，that the up1ift of Mt．Rokko and the
subsidence of Osaka Basin by the Rokko movements proceeded in correspondence to each other．
From the facts that the lower part of Osaka Group c1early participates in these movements，and that
杣gher terraces（corresponding to the mid－P1eistocene Tama terrace in Kanto District）a1so are
displaced in re1ation to the movements，Huzitaαα1．（1965）recognized that the Rokko movements
began from the1ower part of Osaka Group（1ate Tertiary），had their chmax age rather in the1atter
halfofQuatemaワ（including the mid・p1eistocene），and even now are proceeding．
The foot part of Mt．Rokko・1ying between the Rokko Mountains side of up1ifting nature
and the Osaka Basin side of subsiding nature indicates strong gradients between up1ifting and
subsidence，and there are formed not on1y f1exures ofbeds，but also severa11ines of faults．Within the
area of Rokko Mountains a1so there remains the lower part of Osaka Group，much of the part is
tmncated by erosion．Considering from the movements of Mt．Rokko and from the state of the
development of Osaka Group at east and west piedmonts，it．is of course expected that formerly the
lro1ionlurfa11dlvl1opldovlrth1prlllntlu㎜itpartofMt．Rokkowiththlhlightof600m．
22
（iV）Rθ仰θ〃Cθ∫
Huzita，K．，and T．Kasama（1965）：Exp1anatory notes for the geologica1map of Kobe City and its
neighboring Areas．κoゐθCめ1C灼δ∫αGθρρδ，No．16，pp．62＿92．．
1shida，S．，K．Maenaka and T．Yokoyama（1969）：Pa1eomagnetic chrono1ogy of vo1canic ash of the
P1io－P1eistocene series in Kinki district，Japan。∫．0θo1．8oc．∫σρα〃，Vo1．75，pp．183－197．、
Itihara，M．（1961）：Some prob1ems of the Quatemary sedimentaries inOsaka and Akashi areas，
Jap畠m．∫．〃〃．Po1γ陀c〃〃c∫0〃肋αり’びηル。，Ser．G．，Vo1．4，pp．13＿30．
Mitsunashi，T．αα1．（1961）：Maps for Futtsu－Otaki，No．5，sca1e of1：50，000．Maps ofoi1fie1ds and
gas fie1dsin Japan，No，4，0θoム8〃〃．oグ”ρα〃．
Nakagawa，H．，N．Niizuma and K．Hayasaka（1969）：B6s6Pen㎞su1a Cainozoic geomagnetic chrono1ogy．．1．Gθo1．8oc．Jαρ舳，Vo1．75，No．5，pp．267－280．
Takeh砒a，H．（1940）：On the geo1ogy of the oi1fie1ds of Soya－Yufutsu，Hokkaido．8θκウ〃G肋δ，
Vm，3，pp．182＿187．
b．8〃わ∫’dゴ〃9α1‘θ”∫
（i）Kα〃o肋肋（Fig－2・12）
（1）α〃肋εoア肋θ∫θ∂伽θ〃勿りノ肋∫肋
The Kanto P1ain has subsided since the ear1iest Neogene period，and the thick Neogene t0
Quatemary deposits have been deposited there．Especia11y，middle and southem parts of the Kanto
P1ain have unintermpted1y subsided，forming“the Kanto Tectonic Basin”since the Pliocene time，
md is an area of negative g正avity anoma1y1ower than－30mga1（Tsuboi，1954）owing to the marine
formations more than3000m thick．
I（＾NT0MTs CH0sHl PENlN
T＾M＾HILLs MlL収＾1〕ENlN BosoPENlN
ウ ｝・。睾 VW似WWωW、・ 、
灘熟1ボ。§…葦川祭勿灘
』畷＼、・θ。．1l．妻・、荻
竈・一……・1■1レ 肢、．．1＆紗
□Silt，Cl・・ 。 O・ 6暑、 K・・・…1・…w…1…
馬：；二111；lllll二bed〕 ＝景、．孤
鰯・。。一＿・。 今11…・…〆、、、、、。、、、．、、、
…Uncon『ormity FOR＾M l，1トEM 0 ■
一一＿．一一〕lio－pleislocene boundHry M0LLしls〔’s 6 ． O
N1Ml・Gm・p N・1N齪k…ω 」■」i・。d． P［へ・丁 幸 ÷ I（11〈azusa Group I（s1I（oshiba Iく＾1KH冊morl
M1Upper MiuraGroup OF1O『un日 CH＝Chonan
S1Sag田mi Group No＝Nojima 1（K＝1（刮kinokidal Kユ■1Ku『o舳ki S・：Shim。…y・・hi U・1U閉g・ Ko：K・㎞m・1・
B Y1Byobugausa AN：Anegasaki UM＝Umegaso
N＾1Naganuma S E1Senom汕H OT1Oladai
Y＾＝YHbu 一く■ K1wada
Fig．2－12． Stratigraphic section of Kanto Basin．
The marine Pliocene－Pleistocene formations of which the Kanto tectonic basin consists are
named the Kazusa and the Narita Groups．The1owest part of the Kazusa Group in the Boso Peninsula
is tu耐aceous cong1omerates overlying the Kurotaki unconformity，which are succeeded by the
a1temation of sandstone and si1tstone of varying thickness frequently with interca1ated volcanic ash
1ayers；and the uppermost part of the group is the massive muddy sand formation．Biofacies of the
臣・・p…b・thy・li・th・1・w・・mdmiddl・p・・t・，whi1・b…mi・g…iti・i・th・・pP…C・・t…fth・
tectonic basin was once1ocated in the east part of the Boso Peninsu1a through the deposition of the
一23
1ower ha1f of the group，and was1ater removed to the northwest．Towards the end of the deposition
of the Kazusa Group，crusta1disturbance occurred in the who1e area of the Kanto Plain and
consequent1y the“Pa1eo－Tokyo Bay”appeared．The Narita Group composed of sandy sediments was
deposited in the Paleo－Tokyo Bay in the midd1e to upper Pleistocene．The group contains abundant
fossil mo11uscs of neritic to1ittoral speices，and is over1ain by the aeo1ian Kanto Loam（vo1canic ash）
formation．
（2） 一P1ゴocε〃ε一1ηθf∫focθ〃εわo〃〃d”フ
Because the Kazusa Group is a typica1marine sedimentary succession from the Pliocene to the
1ower Pleistocene in Japan and yields abundant marine fossi1s together with the fossi1mammals
（肋肋ρ肋∫ρ肌伽α∫，肋〃∫惚od・η・f．α〃・7αθ，8惚・d㎝o・1ε舳〃∫，・t・・），・・1’i・…pi・i・・sh…
arisen concerning the Pliocene・Pleistocene boundary in this group，though they have not yet agreed
with each other．Asanoαα五（B6s6Research Group，1957；B6s6－Miura Research Group，1958）
studied the planktonic Foraminifera in the Neogene succession of the Boso Peninsu1a and fomd that
the first drop（intensive lowering）ofwater temperature through the su㏄ession was recognized at the
midd1e horizon of the Umegase formation which is characterized by cold water species，αoわなθ7肋α
わoκα〃∫（＝0．肋c伽加7伽）．These authors maintained that this horizon might correspond to the
Pliocene－Pleistocene boundaエy as defined in the18th Intemational Geo1ogical Congress，This horizon，
on the ohter hand，is p1aced near the pyroc1astic key bed U6by Mitsunashiαα1。（1959）。Recent1y
Nakagawaα〃 （1969）carried out the measurement of paleomagnetism of the Neogene t0Quatemary muddy rocks above the base of the Amatsu formation（midd1e Miocene），and correlated a
norma1period found in the middle part of the Umegase formation（near U6）to the O1duvai event in
the Matuyama reversed epoch（Fig．2－13）．From the above－mentioned evidence we can conc1ude that
the P1iocene・Pleistocene boundary of the region is in the midd1e part or near U6・tuff of the Umegase
formation．
1：Orn1…ItiOn Ke｝hcdp■Cun山gllCll；nl
一11｛1■11Hl．Pollじli
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、5 o 一ノニ
■
K；1，；lmいTi
ク ZU11ピ1
1く、1二 o∫■’
〔’hU11」n 三
（1h．弓o ＝
，
o■」＾
1（ユ，klnUkldi■1一・一 7nnじ5
o ＾一一一
Ku二o－I一一
ニゴー
■と㏄
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KOkunlO－O ■一σ■
o 』’’●■ I
1 ；
● llUl」七’
〔1
llll
＝’」
一1
7いnじ．…
● 一一
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一● 引一
一一
1’’Lo O 『
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o llllI○舳dlli ■δ■ ・＾’
；」
027」1∫＾一
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’’6
’L’一〔’’一＝山’一〇一1
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7川1じ1KIwd＝i
1くd3R o 一‘チ
Kuro一；Iki
ONomla1 1．』Hmmillo G一（；j1bor一
●Revcrsc 〇一｛）ld1川111
Fig．2－13． Pa1eomagnetic and paleonto1ogica1chrono1ogy of Kazusa Group．
一24一
（3）〃∫舳〃…ノ1〃1ε抑〃！（・〃1・舳）（w一舳∫f・・θηεわα〃伽・
Accordi11g to lshiwada’s studies on benthonic foraminiferal assemblage in the above
sedimentary succession，the upper horizon of the Umegase formation is characterized by the
assemblage〔）fσ1惚θ〃11ασん肋ε1一∫f∫of bathya1facies，and the base of this fossil zone is p1aced near the
horizon of U6－tuff（Kanel1araα〃．，1958）．Theσl1なε1プηααん〃αε〃∫j∫zone has been recognized at
many test－wells for exp1oitation of the S0／1th Kanto natural gas field，east ofChiba City in the Boso
Peninsula－West of Chiba City，the above fossi1zone is not c1ear1y recognized because the neritic
dwe1lers appear from the1ower horizon，but the base of the Kokumoto formation or the top of the
Umegase formation is wel1－marked by the1ower limit of the warm water foraminifera1assemb1age
such asαoわ07（）吻伽加プ1〃αand G．ぴα∬oプ～〃〃∫etc．（Higuchi＆Kikuchi，1964）．
In the Kanto P1ain the occurrence of t｝le fossil zone in the upPer to midd1e horizons of the
Kazusa Group inc1uding the Umegase romati（〕n was confirmed by the fossi1foraminifera1assemb1age
atadepthofmorethan600mbelowsealevelinatest－wel1atKasukabe（FukutaandIshiwada，1964）。In northem Kanto the base of the upper part of the Kazusa Group or the Umegase horizon is
foundtobe595mdeepinatest－wel1atFujioka（Fukl1ta，1964）．Inthecentra1partoftheKantoPlain，we have no dri11ing that reached t11e Umegase horizon，but the Tama Loam，i．e．the1ower
horizon of the Narita Group，was found at several drilling cores．Assuming that the rate of subsidence
has been uniform，we regal・ded tentatively ltlle depth of the Tama Loam1×5as the basal depth of
the Quaternal’y system．
（4）〃α〃α1〃舳（つ∫∫1必∫〃ακ〃肋19fllθρ〃舳αα
Based on the depth oF the middle horizon of the Umegase formation mentioned in the
preceding section，we can estimate the amount of the subsidence of the Kanto tectonic basin during
the Quatemary・The Umegase formation in the Boso Peninsu1a，however，is not composed ofneritic
sediments，but（）f bathya1ones，so the above－mentioned depth does not indicate the amount of
subsidence of the area」t is necessary to subtract the origiml depth of the formation from the present
one．But the depth ranges detected from fossil records are general1y wide，and moreover，the data
usef111for estimating the original depth of sedimentation are1ittle in the area exc1uding the Boso
Peninsu1a．No correction，therefore，was made in estimating the amounts of subsidence from the
depth ofthe above sedimentary horizon．
Table2－2shows t11e rates of subsidence for different terms since the1ate Miocene in the Kant0
basin which were in胎rred from the thickness and abso1ute age of the formations（Naruse，1968）．In
these estimations the compaction of strata was neglected，and moreover，the origina1depth of the
Umegase formation was tentatively assumed to be500m below sea level（Naruse，1971）．In this table
it is evident that the rate of subsidence became higher since the midd1e Pleistocene than before．
（ii） 0∫αんα〃〃〃（Fig．2－11）
（1）0〃伽θoグ肋θ∫θ”㎜ε〃〃γ肋∫’〃
In the Kinki District there are several fau1t basins，that is，the Osaka Plain，the Kyoto Basin，the
Nara Basin，etc．，which border mo11ntains（）r hmy lands with thrusts．The hilly lands are usual1y
composed of the Osaka Group and its equivalents of the upper Pliocene to lower Pleistocene．These
strata are also distributed under the basins and p1ains overlying the Neogene formations or the
granitic and Paleozoic basement．The correlatives of the Narita Group in the Kanto Plain are
sporadicaHy distributed as terrace deposits covering the OsalkaGroup．
The lower part of the Osaka Group is composed of the altemation of sandy grave1and c－ay of
fluvia1or lacustrine origin，while the upPer part consists of frequent altemations oflacustrine gravel
or clay and marine c1ay（Ma0＿Ma10）or sand．A1arge number of volcanic ash layers are
intercalated，and mammalian bones，molluscs，p1ant remains，pollen and diatoms are also abundant1y
contained．Intensive studies have been done conceming the climatic changes and marine transgression
and regression during the deposition of the Osaka Group and its correlative groups（Itihara，1961．
1966；Kinki Group，1969）．Only a few deep we1ls were drilled in the central part of the plain．The
一25
Table2－2． Rate ofcrusta1movements in the Kanto Tectonic
Basin since upper Miocene（Namse，1968）．
Horizon
Time span（・104y．） Vertica1displacement （m） Rate（m／103y．）
Literature
Base of the Kiyosumi F．一 Top of the Anno F．
1，OOO 1，O00 0．1 Koike，1948
Base of the Kuエotaki F．＿ UmegaSe F．
500 2，000 O．4
Mitsunashiα”1．，1959
Top of the Umegase F． 200 1，OOO O．5
Base of the Na1ita G正oup 50 600 1．2 Kawai，1965
Top of the Narit別Group 1O 130 1．3
Kaizukaασ1、，1963
Yurakucho F、 O．62 7 1．1 Sugimum，1967
deepdri11ingOD－1inOsakaCityrevea1edthebaseoftheOsakaGmuptobeabout660mdeep（Ikebeand Takenaka，1969）．This fact shows remarkab1e subsidence of the p1ain since the1ate Pliocene time。
（2）P〃ocθ〃θ一P1θ’∫τooθ〃θわo〃〃dα7γ（Fig．2－14）
As the Osaka Group yie1ds many fossi1e1ephants and plant remains from various horizons，the
P1iocene・P1eistocene boundary can be defined by using megafossi1s．Itihara（1961）considered that the
Pliocene－P1eistocene boundary was drawn between the1owest part of the Osaka Group which was the
n…i・hi・g・t・g・・fth・〃伽榊・加n…（〃伽θg・・加，吻・・1α，α〃f・∫卯・肋∫，”ψκθ・加㈹・
etc．）and the1oweT part of the group whjch yielded p1ant remains of co1d climate such as〃舳∫
κo肋θ〃∫ね，〃ε〃〃〃加∫，etc．and indicated extinction of〃θ伽θψo加f1ora．His view is main1y based
upon the striking resemb1ance in f1ora1change between the Osaka Group and Ita1ian sedimentary
succession，that is to say，the〃θ肋∫θψo加nora f1ourished in the P1aisancian－Astian stage，whi1e the
indicators of co1d c1imate such asλがθ∫，乃．cω，〃舳∫，励g〃∫，etc．appeared in the Ca1abrian－
Vi11afranchian series（Itihara，1961）．0n the other hand，based on the fossi1e1ephants，the
Pliocene－P1eistocene boundary is drawn between the f1ourishing stage of8κgodo〃α肋∫〃θ〃∫応and航
∫・理．〃伽1・・dth・・pP・・・・・…f肋ρ肋∫∫〃gθ・∫f∫（1tih…，1966）・
Recent1y pa1eomagnetic measurements have been carried out for a number of vo1canic ash
1ayers in the Osaka and Kobiwako Groups，etc。（Ishidaθfα五，1969）．As a resu1t three horizons，i．e．
“Pink・”，“Naka一”and“Kono・H”ash layers，were corre1ated to the Jarami11o，Gi1sa and O1duvai events
in the pa1eomagnetic chrono1ogy，respective1y．A㏄oエding to Ishidaθfαム，（1969），the distribution of
“Kono－H”ash1ayer is reco馴ized on1y in the Kobiwako Group，but“Pumice”・ash1ayer immediate1y
be1ow the “Kono．II” is㎞terbedded in both the Osaka and Kobiwえko Groups．If so，the
P1iocene・Pleistocene boundary can be drawn direct1y above the“Pumice”・ash1ayer of the Osaka
Group．This horizon nearly conesponds to the1owest horizon yie1ding p1ant remains of co1d c1imate
in血e group（Ibaraki Research Group，1966）．Moreover，it is very favourab1e that the“Pumice”一ash
1ayer or its come1ative horizon is we11pursued in the Osaka P1ain and in血e Nara Basin（Kinld Group，
1969）、
（3）凧θ肋∫α1伽ρ肋oア肋θ0∫ακαG70〃ρ舳∂肋θα㎜o〃〃oグ∫必∫”θ〃oε肋肋θρ〃fθ閉〃γ
The horizon of the P1iocene・P1eistocene boundary is we1l recognized in the hi11y1ands around
the Osaka P1ain，but it is difficu1t to con趾m the boundary in the Osaka Group buried under the
26
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Fi8．2－14． Corre1ation of pa1eomagnetic chrono1ogy，biostrati即aphy and c1imatic changes of the
Osaka Group（Ishidaαα1．，1969）
ホ● norma1o reversed Sk：Shinkori warm age，
M：Manchidani co1d age，G：Gokenya cold age，KH：Kamimum II co1d age，K1：Kamimura I co1d age，
S：Seman warm age，T：Terasho co1d age．
一27
plain．Therefore，we adopted the depth of the base of the Osaka Group as approximate amount of
subsidence of the Osaka P1ain in the Quatemary．As to the origina1depth ofthe deposition，it can be
estimated at about O m，and so any correction was not made．
In the Osaka Bay area，the amount of subsidence in the Quatemary boundary p1anes between
the basement and the Osaka Group or the“upper Pleistocene deposits”was revea1ed by sonic
prospecting（11uzitaandKamata，1964）．
（iii）〃o肋〃α加（Fig．2－15）
（1）0〃1加θoグ〃1θ∫〃カηε11伽二11加∫加
The Nobi P1ain is a fau1t・an夢e basin bordered by the Y6r6 fau1t on the west．The
P1io－P1eistocene AgξGroup is distributed in the hil1y lands to the southwest of the p1ain，whi1e the
Seto Group of the same age is distributed in the eastem hi11s．These groups were deposited in the
“Tokai Lake”which existed in the second stage of“Pa1aeo－Seto lnland Sea’’，where the Osaka and
Kobiwako Groups a1so were deposited．ln the Nobi Plain the Ag6and Seto Groups are distibuted
under the ground，and the stratigmphic relation between them is not fu11y known because of the
deficiencyofdeepdri11i・gs．
The AgξGroup is composed of a1temation of non－marine clay，sand and gravel，frequent1y
intervened by layers of lignite and vo1canic ash－In its uppermost part the grave1facies predominates．
〃αα∫θg“o加nora is contained throughout the whole succession，while fossil elephants are sporadic．
Total thickness ofthe AgξGroup attains some600n1in the northem part ofthe hil1s．
v6R6M一．R ＾
． NOBl PLA1N NAG0YA sANAGE ．
’ ・・山・W ・・・・…． ・τ洲舳、。・q1g．∫1 † 冒舳E舳’
、 ＼ 一 ・’＼ ‘2000
Fig－2－15－ Profi1e of Nobi ti1ting b1ock（Kuwahara，1968）．
The Seto Group consists ofterrestrial deposits composed ofgravel，sand and c1ay intervened by
1ignite seams．It is divided into two formations，the1ower being the Seto Porcelain Clay．and the
upper the Yatagawa formation，both of them exhibiting deltaic facies．The Yatagawa formation with
very varied sedimentary facies extends as far as under the Nobi P1ain and is overlain by the Karayama
formation．The thickness of the Yatagawa formation is about250m in the eastem hiHy area
（Matsuzawaααム，1960），becomes thicker towards the p1ain，and exceeds500m．This fact suggests
that westward ti1ting of the basement had already begun at the time of the deposition of the
Yatagawa formation．After the deposition of the Karayama formation，the Nobi Plain proper has
subsided until the present（Kuwahara，1968）．
（2）P〃ocθ〃θ一1干7εゴ∫focθ1κわoα11dαひ，
As the Age Group yields8κg〃o〃θ1θρ11伽ωj此∫fromthe1owerpart，and砒ακα∫〃θ〃∫’∫from
the upper（Takehara，1961）、the Pliocene・Pleistocene boundary is刮ssumed to be at the upper horizon
of the gr（〕up（the1ower part of the Oizumi formation）from the palaeontologica1point of view．On
the other hand，〃舳∫〃伽肋f1ora，an indicator of the Pliocene age，is reported from the1ower
horiz（）n ofthe Seto Group（、the Seto Porce1ain Clay）．
一28
Recent1y the“Pumice”一ash1ayer which is interbedded in the lowe11part of the Osaka group was
reported from both the Age and Seto Groups（Ishidaθfα1．，1969）．Based upon the former discussion
in（ii）（2），we can draw the P1iocene－P1eistocene boundary either near the base of the Oizumi
formation or in the Owari coa1y facies of the upper part of the Seto Group．Though the base of the
Oizumi formation is considered to be500m deep at the Nagasl1ima R－3weH（Research Group for
Low1and Geo1ogy，1966），1itt1e is known about the Pliocene－Pleistocene boundary under the Nobi
P1ain．There is－an opinion that the boundary may be drawn between the Karayama formation and the
Seto Group in the vicinity ofNagoya based upon the po11en ana1ysis（Nagoya Group，1969）．
（3）η1θllo・た・ηαdoμθdα∫わα∫θ∫・〃1θ〃θ肘・・θ〃〃舳α肋・∫加〃1州αρ
As stated above，the Pliocene－Pleistocene boundary can be drawn at the upper part of the Age
Group（and the Seto Group）in the hil1s and is not evident under the Nobi P1ain．As it was pointed
out that the Karayama formation unconformab1y overlies the Age Gr01』p（Kuwahara，1968），a part of
th・fo・m・tionsnea・tll・ho・izonofthePlioc・ne・P1ei・toc・neb・・ndarymaybe・・odedout，
0n the other hand，if we adopt the bases ofthe Age and Seto Groups，these are1ower than the
base of the Osaka Group and their age may date back to the middle P1iocene time．Therefore，we
considered that the base of the Karayama formation is a stratigraphicaHy we11・defined horizon ofthe
P1iocene－P1eistocene boundary，and regarded its depth as the amount of Quatemary subsidence．
（4）Dθρτんoグf灼6わα∫θo∫〃κ1（αrα、1〃〃α∫b7η〃〃o〃
As the data conceming deep drii三ing in the Nobi Plain are so poor that we inferred the basai
depth of the Karayama formation from the depth of its upper horizon，except a few dri11ings
penetrating the base of the Karayama formation．The method of fhe inference is as foHows．Sugisaki
＆Shib・t・（1961）・1・s・i命・dtheg・…lb・d…d・・th・NobiPl・i・i・t・si・ho・i・㎝s・・dfig…dth・
isobases of the second gravel bed（G2）over the whole extent ofthe Plain．Comparing the Sugisaki＆
Shibata’s classification with that of the“Foundation Map of the North1se Bay”（1962），we
corre1ated the G2grave1bed to the uppermost one of the Yagoto formation and the G6grave1bed to
the Karayama formation．As the depth ofG6is about3．5times that ofG2，we regarded（the depth of
G2）x3．5as the depth of the Karayama formation．
（iV）Mな肋〃α加
（1）0〃〃〃εo∫〃1θ∫θ”〃θ〃勿1二γわα∫肋
Many dri11ings have been done in the Niigata Plain and its surroundings for exploiting natura1
gas and oi1fie1ds．But the opinions are different concerning the stratigraphic re1ation between the
・・b…f…f・・m・ti…i・th・…t・・lp・・t・fth・p1・i…dth・g・（・1・gic…c…i・・i・tl・・・・・・…di㎎
M1s．The P1iocene－Pleistocene deposits in this district are named the Uonuma Group which overlies
the Chuetsu Group with partia1unc㎝fo㎜ity and is500to1000meters thick（1kebe，1968）．The
1ower ha1f of the Group（the Tsukayama formation）is mainly composed of a1temation of sand and
c1ay intervened by grave1beds，and yie1ds fossi1s of brackish to neritic molluscs．The upper halfofthe
Group（the Oguni formation）is deposits in brackish to freshwater condition and consists of
a1temation of c1ay，sand and grave1frequent1y intervened by1ignite seams，The Uonuma Group was
deposited on a sedimenta取basin of tectonic orgin after the deposition of oi1－bearing Tertiary system．
Severe folding occurred after the deposition of the Uonuma Group and is now continuting．
（2） P〃ocθ〃θ一P1θf∫τocθηθわoα〃dα1ツ
Lower ha1f of the Uonuma Group yie1ds1∫κgodo〃ακα∫〃θ〃∫ゴ∫together with〃θ伽ε〃o加nora
and has been considered to be1ong to the upper P1iocene to1ower P1eistocene age（Ikebe，1968）．
A㏄ording to the study on the p1ant remains of the Uomma Group in the Oguni area（Mizushimaα
α1．，1970），the Pliocene・P1eistocene boundary may be drawn between the Uomma Group and the
underlying Wanazu formation．Recent pa1eomagnetic study by Nitobe＆Niitsuma for the Uonuma
Group in the same area e1ucidated that the lowest part of the group can be corre1ated to the Gi1sa
event in the Matsuyama reversed epoch（Yamanoiθfα五，1970）．In this case，the horizon of the
Olduvai event may be placed in the Haizume or Nishiyama formation of the Chuetsu Group be1ow
一29一
the Uonuma Group．
0n the other hand，po11en ana1ysis（Yamanoi，1969），pa1aeomagnetic measurements（Nitobe＆
Yamanoi，1970），and fission track dating（Suzuki＆Yamanoi，1970）were carried out for the
Uonuma Group near Tokamachi City．According to these studies，pol1ens of〃θ伽θψoあare
frequent1y contained be1ow the mud－f1ow2（mト2）or at the top of the1ower part of the Uonuma
Group，whi1e mf・2horizon is comlated to the pa1aeomagnetic boundary between the Matsuyama
reversed epoch and the Gauss norma1epoch．Therefore，the Olduvai norma1event is assumed to be at
the horizon s1ight1y be1ow m£3in the midd1e part of the group，and the fission・track age of Surigoma
tuffabove M£3is1．90±0．15m．y．A㏄ording1y，the Pliocene－Pleistocene boundary is drawninthe
midd1e part ofthe Uonuma Gmup in the Tokamachi area．
0n the other hand，seven grave1beds，G0 ＿G6，have been discemed as the natura1
gas－producing beds exten砒ng under the Niigata P1ain．However，as to the basa1horizon of the
Quatemary system under the p1ain，opinions are various and the base of the Quatemary has been
considered to be at G4，G5or G6hodzon．
（3）ノ1η一〇〃〃’oグ∫〃わ∫ゴdθ〃cθd〃1・肋9f〃θρ〃ακ7〃αりノ
Though，as is mentioned above，severa1stratigmphic prob1ems such as the definition and
subdivision of the Uonuma Group and the corre1ation between the group and subsurface gravel beds
in the Niigata P1ain are unso1ved，we figured the isobases ofthe G4bed in the Map，a㏄ording to the
opinions of Ida（1955）and Niigata Prefecture（1957）who corre1ated the G4bed with the boundary
horizon between the Tsukayama and Wanazu formations．Recent1y，Nishida（1969）discussed about
the P1iocene－Pleistocene boundary in the Niigata natura1gas fie1d，whereas our Maps were a1ready
published．After his op㎞ion，the base of the Uonuma Group is considered to be considembly deeper
than the G6bed，and the Pliocene・P1eistocene boundary is assumed to be at a horizon between the
G5bed（500mdeep）andthebaseoftheUonumaGroup（800mdeep）．AsthedepthoftheG4bedis340mdeep，wemustaddsome200mor400mtotheisobasesin血eNiigataP1ain・Thebaseof仇e Tsukay㎝a fomationis fardeeper伽an1000minitsthickareaafterIkebe’sgeo1ogicψro刷e of
the Niigata P1ain．
（V）／∫〃肋〃舳d〃∫肋0PZα肋∫
The Quatemary deposits in Hokkaido are we11developed in the Ishikari Low1and region in the
west and the Kushiro P1ain in the east，but very little is known about the P1iocene－P1eistocene
boundary．We adopted the bases of the so・ca11ed1ower Pleistocene formations as the Pliocene－
P1eistocene boundary in the Map．
In the Ishikari P1ain the base of the P1eistocene deposits is considered to be at the base of the
Noppo正o formation which composes the Nopporo h㎜s to the southeast of Sapporo・The Nopporo
fomati㎝c㎝sistsofa1temati㎝ofsand andc1ayinthe1owerpart，marinefaciesinthemidd1epart，…md of nuvia1gravel，sand and c1ay in the upper part．It becomes thicker under the Ishikari P1ain，
exceeding500matthemαimum（Yamaguchiαα1．，1964）． In the Kushiro Plain，the Kushiro group of the so－ca11ed1ower to midd1e Pleistocene is main1y
composed of marine deposits part1y intervened by non－marine facies，and is more thm500m thick at
the maximum（Hokkaido Group，1969）．
（Vi）伽畑θκθ∫（ホ肋∫αρα・θκ）
Boso Research Group （1957）：Geohistoric division of the Cenozoic formations in the Boso
Peninsu1aホ．γ0κδc乃0，No．7，pp．32－37．
Boso and Miura Rese皿ch Group（1958）：Corre1ation of the Cenozoic formations between Boso
and Mu廿a Peninsu1as by fossi1p1anktonic Foraminiferaホ。γ鮎δc舳，No．9，pp．34＿39．
Department of Construction，Aichi Pref．＆Mie Pref．（1962）：Resu1ts on investigation of the臣ounds
in the northern coasta1region of the Bay ofIseホ．334p．
Fukuta，0．（1964）：Test dri11ing at Fujioka（Pre1im㎞肛y report）＊．α肋〃〃〃θw∫，No．114，pp．
1－1O．
30
＆Y．Ishiwada（1964）：Geology of the Kwmto area，with an intmduction to
explomtion and deve1opment of its natura1gas deposits．∫．∫αραηλ∬．1〕θ〃o1．τεc乃〃．，No．29，
pp．3＿21．
Higuchi，Y。＆Y．Kikuchi（1964）：Microbiostratigraphic study of the Kazusa Group specia1reference
to its natura1gas resou1＝ces．∫．∫αραηλ∬．Pθ卯o1、τεc〃η．，No．29，PP．22－28．
Hokkaido Research Group（1969）：Quatemary system of Hokkaido｝．ρ“ακ閉〃γ収〃θ㎜oグ．1αρσ〃，
PP．1－34．
Huzita，K．＆S．Kamata（1964）：Geo1ogy of the Osaka Bayホ。Clo㎜棚他θ拘〃加8o〃c1〕70“ρθc伽8
ル7肋ε0〃κα3αγ．
Ibaragi Rese町ch Group（1966）：The Osaka group of Fukui area，north of Ibaj＝agi，0saka Prefecture，
and occun＝ence of亙1θρんα∫∫んをθ〃∫な ㌻P1‘oグ〃．ル伽f∫〃∫乃〃α，〃θ閉o’．加1κo〃〃θ，PP．117－130．
Ida，K．（1965）：Geo1ogy of the Niigata gas fie1dホ．3“1五Gθoム8〃．∫αρα〃，No．6，pp．327＿342．
1kebe，Y。（1968）：Tectonic district，Niigata Prefecture，Japan竈．〃θ㎜．Gθ〇五∫oc．．1σραη，No．2，pp．
43＿47．
Ishida，S．，K．Maen出a，＆T．Yokoyama，（1969）：Pa1eomagnetic chronology of vo1canic ash of the
P1io－P1eistocene series㎞Kinki district，Japaバ．。1．Gθoム8oc．．1αρσ〃，Vo1．75，pp．183＿197．
Itihara，M．（1961）：Some prob1ems of the Quatem趾y sedimentaries in the Osaka and Akashi町eas，
Jap皇m．∫．伽Jf．Po1〃εc乃．0〃κoα卯σ”加．，Ser．G，pp．13＿34．
（1966）：The Osaka阻oup and Rokko movements“．α汰〃Kα幽κωr亙α〃乃8cた肌θノ，Nos．
85＿86，ppl12＿18．
Kaizuka，S．θfα1．，（1963）：Geomorpho1ogy of Japaバ．α敏κ〃Jδ肋o19，CI〃幽κ“一伽〃αゴーκθ枇γ〃σゴ
μ∬．Gθo1．Co〃αρ．∫αμ〃ノ．
Kaneh町a，L．，K．Motojima，＆Y．Ishiwada，（1958）：The naturaI gasホ．361p．λ〃κ〃α舳o化ηTokyo．
Kinki Research Group（1969）：Quatemary system of K㎞ki districド．ρ〃〃θ閉〃γ〃∫κ㎜oグ．1αραη，
pp．331＿354．
Koike，K・（1948）：Geology of the midd1e part of the Boso Pen㎞su1a（I）．3〃1．1〕妙∫’og〃ρ〃cα18cj．
Rω．〃∫f．τoκγoσ〃ル．，No．3，pp．1＿6．
Kuwahara，T．（1968）：The Ncbi bashs lmd its fau1t b1ock movement＊．ρ〃〃．Rω．，Vol．7，pp．
235＿247．
Matsuzawa，I．α〃（1960）：Gθolo馴oグ肋θ3o〃肋wθ∫fぴ〃肋〃o〃加8α〃昭θ一ヅα㎜α〃〃∫ヤCommittee
of Education，Aichi Prefecture．35p．
Mitsunashi，T．，N．Yasukuni，＆Y．Shinada（1959）：Stratigaphica1section of the Kazusa Group a1ong
the shores of the Rivers Y6r6and Obitsuホ．〃〃11．0θo1．8〃．∫oρα〃，No．1O，pp．83－98．
Mizushima，R．αα1．（1970）：0n the Uonuma formation in the Oguni area．．1．Gθo1．8oc．∫αραη，Vo1．
76，pp．83．
Nagoya Group（1969）：The Quatem肛y system of the Ise Baゾ，ρ〃〃θ川〃γJγ“θ㎜oグ∫αρα〃，pp．
319＿329．
Nakagawa，N．，N．Niizuma＆I．Hayasaka（1969）：Late Cenozoic geomagnetic chmno1ogy of the
Boso Peninsu1が．∫．Gεo1．8oc．∫αρα〃，Vo1．75，pp．267＿280．
Namse，Y・（1968）：Quatem趾y crusta1movements in the Kanto regionホ．〃θ閉．oθoム8oc．．1αρση，No．
2，pp．29＿32．
（1971）：Rate ofNeogene md Quatemary cmsta1movements in the B6s6Pen㎞su1a．0〃肋
Kθ〃α1Ro〃∫肋，No180，pp．228＿245．
Nigata Prefecture（1957）：Report of the geo1ogic suπey for the natura1gas recources‡．〃晦α吻〃εノ1
Nishida，S．（1969）：Formation of the Niigata P1ain and re1ated prob1ems‡．Dα肋3加α1b7肋θ
8γ閉ρo∫加閉 “0oσ∫勿1P伽肋olJαρα〃’二PP．53－58．
Nitobe，T。＆T．Yamanoi（1970）：Pa1eomagnetic measurements of the Uonuma Group．λわ〃αc如oプ1 ραρε7∫7εα∂δθ∫b7θ’乃ε（；θolo叙1cσ18o dθ’γo∫’．1αραηα’チ乃ε77f乃ノ1ηη〃α1閉θθf肋8，PP．121．
Resea1－ch Group for1ow工and geo1ogy（1966）：The Nobi P1aiバ．C〃肋伽〃〃εw∫，No．143，PP．18－27．
Suとimum，A．（1967）：Uniform rates and duration period of Quatemary earth movements in Japan．∫
Gεoκゴ．0〃肋α卯σ〃加．，No．10，pp．25＿35．
Sugisaki，R．＆K．Shibata（1961）：Geochemica1study on ground water（I），Subsurface geo1ogy and
一31
aquifersin the N6bi P1a㎞＊．ノ、Gθo’．∫oじ．ノαρα〃，Vo1．67，pp．335一一345．
Suzuki，M．＆T．Yamanoi（1970）：Fission track dating of the Uonuma Group．ノ、（，θo1－8oc．．1αρα〃，
Vo1．76，No．6，PP．317－318．
Takehara，H．（1961）：Stratigraphy of the Age group，ηorthem Mie Pref．，Japan．〃oプ1∫〃α々γαη〃
”ε1η0”α1一／01“榊θ，pp．45＿50．
Tsuboi，C．（1954）1Map of Bouguer anomaly distribution in Japan based on apProximate1y4，500
measu「ements．倣”亙α”畑．Rθ∫．／1耐、，Suppl．Vo1．4，pp．125一一127．
Yamaguchi，H．αα1．（1964）＝Explanatory Text of the hydro1ogica1maps of Hokkaido No．8，
SapPoro＊．（≡θo1，8o〔・．／／‘）んんαfdo．
Yam㎝oi，T．（1969）：Pollen fossils from the UonLlma Group（T6kamachi City area，Niigata Pref．）一
Dαfα ∫乃εθ工 o∫．f乃θ 8γ1ηρo∫’〃η一 “（■oα3fα1 P1αf〃” 乃ε1d αf 〃1～ 76〃一 、41〃η〃1 ハfθθ〃〃9 o∫一fんε
Gθologfco18ocたひ1‘）∫’∫αραη，PP．199一一202．
，S，Ueno，＆T．Nitobe（1970）：Some problems on the Pleistocene Uonuma Group in
NiigataPrefecture＊．τ乃θρ“ακ川αり・Rε．∫θακ＾，Voし9，pp．134一一一138．
2．3．Synthesized map of vertical disp1acement
It is found by a comparison of the amounts of Quatemary vertica1displacement estimated
by geomorphologica1method with those estimated by geological method that the re夢ona1
distributions of these amounts genera11y show simi1ar modes in two maps－There are，however，some
regions where the amounts and the modes of their distribution are quite different in each of the two
maps，because the amounts estimated either geom（〕rphologica11y or geologica11y were obtained from
uncertain dat刮、In genera1，the amounts geomorphologica11y estimated tend to be by200to300
meters1arger than those estimated by geological method．This is reasonab1e，because most of the
amounts geologica11y estimated are based on the upper Pliocene marine formations which were
initia1ly deposited on the surfaces lower than contemporaneous subaeria1erosion surfaces and have
been much denuded in m（〕untain areas．
Considering the limits of these two methods and the above－mentioned differences of the
amounts in the two maps，the Map No．3was synthesi7ed什om the MapsNos．l and2，Inthismap，
degrees of vertical movement were classified into ten／ones of is（〕一disp1acement，six being uplifted
areas djvided with250－m，500－m，750－m，1000・m，and1500－m isopleths，and four zones being
subsiding areas divided with250－m，500－m and1000－m isop1eths・
In areas where the amounts estimated by the two methods be1ong to different is（〕一displacement
zones，it was examined for the initia1data which of them were based on more certain proofs．And
fuれher，in mountain areas the amounts geomorphologica1ly estimated were geneml1y used，because
erosion surfaces extensively extend and Pliocene or Pleistocene fornlations are poorly distributed
there．On the countrary，the amounts geological1y estimated were app1ied to piedmonts and hills，
because extensively distributed Pli（〕cene and Pleistocene formati（〕ns have not been denuded so much
・・dp…1ydi・t・ib・t・d…si・・…f…sh…f・・q…t1yb… di・1…t・dbyf・・1ti・gth・・e・I・
remarkab1y subsiding areas，amounts of subsidence cou1d be estimated only by geologica1method．
Erosion surfaces fornled in the 1ate P1iocene or early Pleistocene are not distribute d in the
centra1parts but on1y in the margina1parts of the Kilakami，Kii and S11ikoku Mountains and others－
In the central parts of these mountains，however．older erosion surfaces can be found．The amounts
of Quatemary vertica1disp1acement for the㏄ntral parts were estimated by assuming an imaginary
extension of the1ate Pliocene or ear1y Pleistocene erosion surfaces in tl1e nlarginal parts paraHe］to the
older erosion surfaces．
2．4．Regiom－chamcteristics of Quatemary vertical displacement
（1） Up1ifts throughout the Quatemary are n1ost remarkab1e in Centra1Japan where the
Japanese alps are located and the maximum va1ue of the up1ift attains1700meters in the Hida Rmge．
Amounts of up1ift rapid1y decrease in the n1argina1part of Centra1』apan一
（2） Up1ift in the Quaternary amounts to 1000meters in the Hidaka，Yubari and Echigo
Ranges and in the Uonuma，Kii，Shikoku and Kyushu Mountains，but the amounts are less than750
32
meters in the Kitakami，Abukuma and Chugoku Mountains and in the no正them part of Hokkaido．
（3） Throughout the Japanese Is1ands the amounts of up1ift in the Quatemary exceed ha1f the
present height of mountains and in some regions reach even about two thirds of the1atter．The
present altitudes of the Japanese Islands，therefo正e，are most1y due to Quatemary crusta1movement．
（4） Large p1ains in Japan such as Kanto，Nobi，0s水a，Niigata and Ishika正i P1ains are subsiding
regions and amounts of subsidence in the QuatemaW attain1400meters in Kanto P1ain，700meters
in Osaka Plain，600meters in Ishikari P1a㎞and500meters in Niigata P1ain．These subsiding regions
are structum1basins，of which margina1parts have㎞gh gradients of Quatemaワvertica1disp1acement，
rapid1y descending from up1ifted regions to subsiding ones．
（5） Amounts and modes of Quatemary vertica1disp1acement are remarkab1y different
between the northeastem and southwestem parts of Japan divided by a1ine from Ise Bay to Wakasa
Bay．In Southwest Japan，amounts of vertica1disp1acement are much1arger in the Outer Zone than in
the Imer Zone and rapid1y decrease northwards a1ong the Median Tectonic Line，by which the lnner
and Outer zones are divided and a1ong which fau1ting has occurred in the Quatemary at severa1
locations．In Northeast Japan，however，the difference of vertica1disp1acement between its eastem
and westem parts are not so remaエkab1e as in Southwest Japm．
（6） In Northeast Japan，vo1canoes are genera11y distributed in arcuate zones paral1e1to the
is1and arcs，where the heights of mountains and the amounts ofQuatemary vertica1disp1acement are
larger，and the axes ofup1ifted areas in the Quatemary are located a1itt1e west of the eastem margins
of the vOlcanic zones．
（7） Amounts of vertical disp1acemnet do not genera11y vary so much in sma11extents which
are surrounded by marginal zones with high gmdients，though they are remarkab1y different ih
various regions of Japan．From this fact it is possible to divide the Japanese Islands into some tectonic
regions acco正ding to Quatemary tectonic activities，These tectonic regions have probably a c1ose
re1ation with regional characteristics of recent seismic activities，as wil1be mentioned1ater．
3．Quaternary fau1ts and folds
In the maps of Quatemary vertica1disp1acement，1inear or arcuate parts of high gradient may
have resll1ted from Quatemary fau1ting or f1exure，but small Quatemary faults are not genera11y
expressed in these maps．On the other hand，up－and down－warping with1ongwave1ength are shown
in these maps as uplifted and subsiding areas，respective1y．Sma11folds with short wavelengths and
smal1amp1itudes，however，are not found in these maps．
Many faults and folds which have been more or1ess active in the Quatemary have been
discovered in various regions of Japan and a c1ose relationship between their distribution and recent
seismic activities has been recognized．That is，regions where fau1ts were active in the Quatemary but
any great earthquake has not o㏄urred in the recent time have a higher probabi1ity of outbreak of a
destructive earthquake in near future than those where it o㏄urred recent1y，From this reason it has
been considered that distribution maps of Quatemary fau1ts and fo1ds are very usefu1and
indispensab1e for finding out the regions where great earthquakes may o㏄ur in near future and，
according1y，various observations of present seismic activities should be carried out for prediction of
earthquake s．
Fr6m this point of view，the Research Group for Quatemary Tectionic Map has co11ected data
on Quatemary fau1ts and folds in Japan and compi1ed these separate1y in two distribution maps on a
sca1e of l：2，000，000（Maps Nos．4and5）．
3．1 Quater11ary fau1ts
3．1．1．Method
Quatemay fau1ts as defined in this paper are those which have dislocated upper P1iocene or
younger formations and geomorphic surfaces，刮nd have caused seismic fau1ts more than1km1ong．
Such faults were picked up over the Japanese Islands，using geo1ogica1maps of various sca1es
33
published by the Geological Survey of Japan and other organizations，and geo1ogica1and
geomorpho1ogical maps contained in scient椚c papers．558Quatemary fau1ts were picked up in the
abovementioned processes，were listed up as shown in the appendix，and were numbered in eveW
quadrang1e of the topographica1map on a sca1e of l：2，000，000．Among them，132faults were p1otted
in the Map No．4，excluding those1ess than10km long and those which have not been ascerta㎞ed
but only inferred，because the scale of the distribution map was too sma11to contain a11the
Quatemary faults picked up．
In regions where fault nets are very comp1icated，para11el fau1ts more than two were represented
by one main fau1t and at some places those1ess than15km1ong were exc1uded in the map．In a part
of Boso Peninsu1a where there develop many para1lel faults trending from north to south and dipping
either eastwards or westwards，the group of these faults was expressed by a hatched area．And
further，the fau1ts which mainly dis1ocate vertica11y are expressed with comb・1ike marks，and those
which mainly dislocate horizonta1ly with arrows．
3．1．2．Examp1es
a．〃θ〃力〃
（i）〃伽伽〃∫c〃ρ
Fig．3・l shows the Gipfe1fur map of a part of Central Japan，the area being situated70km
F…
D．、獲
擁0 5 10 15 20km
Fig．3－1．Gipfe1f1ur map of the Kiso River va11ey。
KF：Kiso－Fukushima
I： Ina
A： AgematsuG： Ge工o
S： Sakashita
Id1 Ida
M： MagomeN： Nakatsugawa
MK：Mino－KamoOn： 0ntakesan
Ks： Kiso Mountains
At： Atera Mountains
EB： Ena Basin
EM：Ena MountainsMk：Mikawa Plateau
FM：Futatsumori Mountains
34
northeast of Nagoya．In the midd1e of the map，a fairly f1at topography s1opes down to the
southwest，and reappears in a lower leve1beyond the steep s1ope．This s1ope has been ca11ed the Atera
fau1t scarp by some geomorpho1ogists（Tsujimura，1929；Okayama，1930；Ito，1941；Kaizukaααム，
1963）．Aseriesoffaultva11eys，separatedbysevera1in・va11eydivides，runatthebaseofthefau1t
scarp．At several p1aces stream channels are offset，suggesting that the area northeast of the fua1t has
moved relative1y by7－10kilometers to the northwest in respect to the southwest b1ock．
TheAterafaultisexpresseda1sogeo1ogica11y（GeologicalSurveyofJapan，1961）．Aconspicuous fault zone is observed a1ong the fault scarp in the1ate Cretaceous rhyo1itic we1ded tuff．
The fault zone consists of fractured rock more than10m wide with a central zone crushed into sand
grainS．
（ii）8σたα∫〃rα伽〃∫ωγρ1α（Fig．3・1）
Near the southeastem end of the Atera fault，at Sakashita，the Kiso River crosses the fau1t1ine，
and severa1river temces have been formed，These terraces are cut by the fau1t and a fau1t scarplet is
observed．Sugimura＆Matsuda（1965）measured the vertica1and horizonta1disp1acements of the
fault，from the offset of the terrace surfaces and scarps（Fig．3・2）．Five displacement vectors were
ca1culated in the fau1t p1ane．They show that（1）the horizonta1disp1acement is about five times as
1arge as the vertica1；that（2）the fau1ting，to date，has been persistent1y left latera1；and that（3）the
rate of faulting seems to be about5meters／1000yea正s on the basis of radiocarbon dating for the
VIHth terrace，27，000ye町s B．P．
ぺ
外
φ ・一 ぺ
■
小“
伽
＼ 帖
㍉勿勿
へ
ぺ
ぺ
“’
ぐ／
““／ 、
Fig，3・2． Diagram showing that Atera fau1t cuts seven steps of river terraces
at Sakashita（Revised from Sugimura＆Matsuda，1965）．
The Roman numerals indicate the numbers of terraces．
The vertica1sca1e is exaggerated five times．
（iii）8〃伽一∫〃ρ伽1岬∫κ閉
Ten or more strike－s1ip faults have been formed during earthquakes in Japan（Arabic mmem1s
in Fig．3－3）and show c1ear1y that（工）a11horizonta1displacements are larger than the vertica1ones in
the same fau1t；that（2）there is no regularity in the sense of vertica1separation of the upthrown
b1ock；and that（3）north－south and northwest－southeast trending fau1ts（nos．3，5，6，7，8and10in
35
Fig．3－3）a正e exc1usive－y1eft－slip，whereas the east－west and northeast－southwest ones（nos．1，2，4and
g in Fig．3・3）are exc1usively right・latera1．
Quatemary active faults（Roman mmera1s in Fig．3－3）inc1uding the Atera fau1t（no．V in Fig．
3－3）show the same characteristics as those of the earthquake fau1ts．1t seems to us that these fau1ts
foTm a conjug田te set of two different shear p1anes，which may be derived from the west・northwest or
east－southeast trending compressiona1stress。
135 136． 1381
自
ノllへ
＼10
5、
〉’ 、Xこ
1夕
し4 辿
＼1・1＼ 芸
lX
■4、．｝
、ll㌦、、
、、
一’
刈
0 1OO㎜
36、
34’
Fig，3－3． Strike－s1ip fau1t system in centra1Japan．Arabic numera1s
indicate scientifica11y observed fau1ts associated with major
earthquakes；Roman numera1s indicate Quatemary active fau1ts一
（iV） 1～θ∫θ7θηCθ∫
Geo1ogical Survey of Japan（1961）1Iida，Geo1．map of Japan，sca1e1：200，000，0saka no．1．
It6，R．（1941）1Some observations in the Atera fau1t va11ey．Gθogγ．Rθll．，Vo1，17，pp．850－855（肋
∫αρα1一ε∫θ）、
Kaizuka，S．，Machida，T．，Ota，Y．，Sakaguchi，Y．，Sugimura，A．and Yoshikawa，T、（1963）：
Gεo閉07ρ乃olo馴（）∫∫αραη．κ〇五1．Chigaku Dantai Kenkyukai，Tokyo，pp．93－98and pp．115－
116（肋∫αραηθ∫θ）。
0kayama，T．（1930）＝Some relationships between recent earth movements and topography－Gθo肌
RθリI，Vo1．6，pp．992＿1004（加。1αρo〃ど∫ε）．
Sugimura，A．＆Matuda．T．（1965）：Atera fau1t and its displacement vectors．Gεo1．8oc．λ㎜、肋〃。，
Vo1．76，pp．509＿522．
Tsujimura，T。（1929）：Gεo㎜07ρ1－olo叙ヒα11）θ∫c〃μゴo〃oグ∫αρα〃．Kokon Book Co．，Tokyo，pp・
223＿226（fη∫αρα〃θ“｝）．
b、〃oわ〃α＿0〃〃〃θα
（i）〃γ0∂〃f0〃
The eastem part of the B6s6Peninsula is，in general，ric11in small faults and joints．The sma11
fau1ts of this area are divided into the following series：
Younger east－west normal fault series，
一36＿
Younger north－south normal fault series，
Reverse fau1t series，
01der east－west norma1fault series，
01der north－south norma1fault series．
（ii） （；ε0108γ
The Boso Peninsula has in its centra1part a horst－1ike structure，whjch consists of strata of
Miocene and older series distributed in an approximately east－west direction，and cut by many fau1ts
with east－west strike．Younger strata are distributed on the south and north sides of the“horst”．As
to the north side，there are strata with east－west and northeast－southwest strikes，and the fo11owing
strata with north dip1ie one upon another in d1e order from be1ow：Miura Group（the midd1e and
upper Miocene），Kazusa Group（P1iocene），Sagami Group（Pliocene－P1eistocene）and Narita Group
（P1eistocene）．
（iii）肋〃げwθ㎜
The older north・south normal fault series are the o1dest among the above－mentioned series，and
their properties are not yet clarified．The o1der east－west normal fault series are distributed in the
southem part of the Boso Pen㎞su1a，and the reverse fau1t series are formed during the younger and
older periods，and a1so deve1oped in the southern part of the peninsu1a．Both the fault groups are
infened to have a relation with the uplift movement ofMineoka＿Hayama zone in the central part of
the Boso Peninsu1a，and to be formed in the middle P1iocene epoch and in the period from late
Pliocene to ear1y Pleistocene，respective1y．
The faults in Mobara and Otaki natural gas fie1ds（Fault No．66－1）shown on the Quatemary
Tectonic Map are those be1onging to the younger epoch and a part of them is shown in Fig．34．As
this area be1ongs to the Mobara and Otaki natural gas Oeld regions，geologica1features have been
studied in detai1．Al1the strata be1ong to Kazusa Gmup，and are chief1y composed ofa1temations of
snad and silt，with many thin1ayers of tuff between them．Strike is here in the direction ofNE・SW，
showing the dip of a few degrees to ten・odd degrees to northwest，As is seen on the map，younger
north・south normal faults are deve1oped the average interva1being200m．Fau1ts with subsiding sides
on the east are predoninating and o㏄upy more than80％，the dip ang1es being steep and over60．
Thethrowsarehard1yover1m，butthosebelongingtothisseriesarelargerthanthoseofotherseries，and are more than20m at the maximum，Most of the fault lines are of sharp straight line type，and
are genera11y accompanied by lens・shaped fault gouge composed of pu1verized fine particles of both
sides．The faults are of dip・s1ip type．They cut the Kazusa Group probably in the ear1y and midd1e
P1eistocene epoch and seem to be re1ated with the regional uplift in the South Kanto district．
In addition，the fau1ts belonging to the younger east－west fault series，which are formed more
recently than the above series，are often observed in coasta1zones of the eastern part of the area
shown on the map．The strikes offaults are nearly paraHel to those ofstrata，and most ofthe fau－t
planesareeitheropenoraccompaniedbyfracturezones．Thethrowsaregenera11y1essthanl m，andless thm2＿3m at the most．It seems that these faults are fomed at the end ofPleistocene and may
be re1ated with the development of the uplift parts in the periphery of the Kanto structura1basin．
（iV）Rθ仰θ肌θ∫
Ishida，Y．et a1．（1971）：〃o肋〃，Geo1ogical Maps of the Oil and Gas Fie1ds of Japan No．10，Geol．
Sur．
Mitsunashi，T－et a1．（1962）：F〃∫〃一0〃〃，Geo1ogica1Maps of the Oi1and Gas Fields of Japan No，4．
Geo1，Sur．
Kinugasa，Y．et al．（1969）：The Minor－fau1t System on the Coastal Area of the Eastem Boso
Peninsu1a．3”1．Gεo1，8〃．∫αρ〃一，Vol．21，pp．13＿38．
C．肋舳∫肋0肋〃伽〃ακε伽〃
（i） ／η卯0d〃C〃0〃
Matushiro Earthquake Swarm（1965一 ） occurred on the edge of the Central Be1t
37
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一38
of Up1ift which had upheaved as the earliest ofthe be1ts in the Fossa Magna．The epicentra1region is
about40km in NE－SW direction and about15km in NW－SE diTection．The hypocentra1depths are
sha1low and concentrated mostly into the depths of2－7km，The number of fe1t earthquakes
hitherto has reached more than60，000．In the seismic activity ofthis earthq｛ake swarm therewere
severa1periods－oξe1evated activity．The seismic activity was most active in the2nd period of activity
（March－Ju1y1966），over600earthquakes a day at the peak・Hypocentra1region showed a tendency
of decrease of hypocentra1depth with the increase in the number of seismic activity pediods，name1y，
in the3rd period of activity（August－December1966），at Matsushiro Basin，the o㏄unence p1ace of
theea・thq・ake，ther・occ・・redext・ao・di・・lc・・sta1n・ctu・tionssuchas・phea・a1・，exp・・si㎝s，
・ontmcti㎝・，a・dt1ting・fthegrou・d；P1entyofgr・md・…k・alsoo㏄・med，andintheneighborhood of cracks there gushed out about ten mi11ion tons of ground water（hot springs）．Some
of the cmcks formed horseshoe shape，and these cracks were due to1ands1ides which o㏄umd in
relation with gushes of ground water．Other crakcs，independent of the topography，were regularly
distributed，and they are considered to be expressions of the fau1ts associated with earthquakes which
occul＝red under the surface soi11aye1＝．
（ii）0cω1γε肌ε
Ground cracks relating to earthquake fau1ts form zones of fissures rangingθ〃θo加1o〃．These
fissures are re1ated respective1y to the1eft－1ater刮or to the right－1atera1fau1ts，the forme正o㏄upying
the greater part．A1eft・1atera1fissured zone a1so is distributedθ〃θc加1o〃in the mnge0．5km wide
and4km1ong．Among these fissures the foremming ones occurred at the peak of the second period
of activity．And according to triangu1ations，in the b1ocks on the both sides of this fissured zone a1so
there are shown the1eft－1atera1and open movements the same as in the ground cracks．A1arge
quantity of ground water gushed out in the阻ound crack zone，and on the extension1ine of the zone
a1so there are some places where the gushing・out of ground water o㏄urred．From these facts it is
considered that this ground crack zone is the area of earthquake fau1ts w㎞ch have occurred in the
basement．The principla geo1ogic e1ements of this zone are considered to be as fo11ows：strike of
N5チW，1eft・1atm1move of500m，extension of7km，vertica1dip，subsidence of15cm on northem
side，and opening amount of30cm．
A㏄ording to the e1ectro－optica1distance measurement for the expansion and contraction ofthe
g正ound，the same tendencies of east－west contraction md north－south extension are a1so c1ear1y
shown，and in the3rd period of activity at the maximum，extension of more than107cm was
observed for the distance ofabout3km in north－south direction which invo1ves the above－mentioned
fau1t．
（iii） 7iθCf0〃た∫θ〃肋9
The Matsushiro earthquake fault has o㏄urred in the centra1part of the hypocentra1region，
with a direction near1y perpendicu1ar to the direction of the1ong axis of the region．The earthquakes
of Matsushiro Earthqu水e Swarm o㏄uned extremely frequent1y in a1imited area，and their
earthquake mechanism is considered as fol1ows：the principa1pressure is of quadrant type ofeast－west
direction，and its noda11ine of the same direction as that of the fault．This earthquake mechanism
shows the same tendency with those of the earthquakes in Centra1Japan．The Matsushiro fau1t also，
as is mentioned above，is a left・1atera1strike－slip fau1t，and this shows that the fau1t be1ongs to the
geo1ogical system the same as that，to which the active fau1ts in the Quatemary at the Chubu District
be1ong（see Fig．3・5）．Furthermore，the ground water which gushed out in the ground crack zone
became hot springs of CaC12－type；there are recrods of gushing－out i』l the past on the extension1ine
of the fau1t；and there are a1so some p1aces showing1ands1ide topography simi1ar to those recent1y
made by the gushing・out．As it seems that earthquakes had occurred in this region in the past，so it is
considered that the Matsushi正o earthquake fault was active a1so former1y．However，geomorpho1ogi－
ca11y speaking，the southem side of the fau1t seems to have subsided，un1ike the recent displacement一
一39
“三
㌧
！ 。 ク 匂事 ㌻～．？ノ1 冬
〃・・一、．二．い
∵・ へ
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、
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／
＼／
／＼．．
㌔
㌔
戸／」
』 冒 市o o ω
』H Φ① 自 でoρ ．2N
雨
筥 づ9づ o冒①
毒 sζ ①』二 一〇 〇； と；…参 ①・εo
司 ’一 』 ⊆ do o’一 ⊆’ 冒’一 目一昌 o ω 』 ．一 ・一 ①o o⊆ O O－ q旦o 233’§パξ看ξ童；5εき8ξ看①畠α；』。。．…2o oき旦〇一〇一〇．貢勺O O’O冒一 ① 閉 記o。｝ 一 』閉づ一』①①』づ◎2…盲oωq＝o b0；・…一昌二ξ
NΦ｛oi1…ε1妻
ε老×①晶ω一〇有．望’ ω 〇一〇勺 一 ① ■①｛目』 d ⊆ 冒 ◎〇一ζ・一川 o ω ωi自一〇①Φ○ 冒’・一勺 ・一 ω一一 〇 一一・一づ一τ づ
婁簑碁o o←国o■｛
．尋
一
／■
（iV） Rθ1ε7ε〃CθJ
Takahashi，H・（1969）：Seismic activity in the post－th辻d period of Matsushiro EaIthquake Swarm and
some recent prob1ems of research．Rερo舳oア0ooρθ〃伽θRθ3ωκん∫071）ゴ∫ω肋〃θリθ〃ゴoη，
No．18，pp．117＿121．
Tsuneishi，Y．＆K．Nakamura（1970）：Fau1ting associated with the Matsushiro Swarm Earthquakes．
8〃1．E〃肋q．R肌1η〃．，Vo1．48，pp．29＿51．
3．2．Quaternary fo1ds
3．2．1．Method
Quatemary folds as denned in this paper are those with wave1engths from500m to30km，
deforming the upper P1iocene or younger formations and geomorphic surfaces．Such fo1ds are
investigated by using geological and geomorphological maps of various scales published by the
Geo1ogical Survey of Japan and others or contributed scientinc papers．Quatemary fo1ds with
wavelengths more than30km1ong are genera1ly expressed as extensive1y uplifted or subsiding areas
一40＿
in the maps of Quatemary vertica1displacement（Maps Nos．1，2and3）．Ho1ocene folds as well as
geodetic folds revealed by precise leve11ings are not contained in the Map No．5，because it is too
difficult to discover a11of them by the geo1ogical and geomorpho1ogica1methods．
About80Quatemaワfo1ds se1ected in these processes are listed up as shown in the Appendix，
and each one coup1e of antic1ine and syncline or gmups of these coup1es in regions where exist so
many folds are separately numbered in every quadrang1e of the topographica1map on a sca1e of
l：200，000．About one third of these fo1ds were revealed with deformation of terrace surfaces．A11of
these fo1ds are plotted in a map ofJapan on a sca1e of1：2，000，000（Map No．5）．
3．2．2．Examp1es
As is above－mentioned，the Quatemary fo1dings shown in Map No．5were detected from the
deformed upper Pliocene or Pleistocene formations and geomorphic surfaces．Strongly fo1ded upper
Pliocene or1ower Pleistocene fom1ations are general1y expressed on some1arge－scale geo1ogic maps．
As for the upper P1eistocene fo1d，the deformation in the upper P1eistocene formation is，in genem1，
too small to represent its folded structure by stratigraphic research．For the representation of folding
in this case，it is useful to study the topographic expression of fo1d on geomorphic surface，especia1ly
On terraCe SurfaCe．
In the fol1owing，three examples of Quatemary fo1d are il1ustrated，a11of them having their
topographic expressions．The1oca1ities of them are shown in Fig．3－6．
28’ 1‘j’ jδ工
μ’
L ＿
1 － O 、 ’’1
1■仁． 一外
1｝
40■
3ポ
V0
辻4
㌶．
∵で冷
“ 午パ
！・ ノ く 一一一†一1・∵㌻しぺ、 ∴一一一しダ ㌧
■一
ソ
Fig．3－6， Distribution of anticlina1axes of Quatemary fo1ds in Japan，with
localities of Figs．3－7，3－8，3－9．
一41
a．〃敏吻〃ω（Fig．3・7）
Niigata area has strongly fo1ded P1io－Pleistocene strata and deformed temce surfaces．In1942
0tuka and Ikebe independent1y disc1osed that the fo1ding of this area is active at present，based on
the evidences of defomed temces and repeated1eve1ing data．Thereafter，many works have been
done for the active fo1dings of this area by geo1ogic，geomorpho1ogic and geodetic means．
The fo1ded strata，making h汕y1and of the Niigata area，are the P1io－P1eistocene Uonuma
Gmup，of which a1most a11antic1ines and sync1ines show coincidence with ridges md vaneys，
respective1y．River terraces in various upper Pleistocene ages have their deformed features as we11．The
landforms of these terraces are studied recent1y by Ota（1969），and are c1assi行ed into eight leve1s
（A＿D）．The deformed temce surfaces are shown in Fig．3－7with restored contours．Cross sections of
these deformed terraces and the under1ying fo1ded Uonuma Group are a1so presented in Fig．3－7．
From these evidences，it was conc1uded that through the upper P1eistocene，the terrace surfaces
have been deformed in the same mode with the fo1ded stmctu正e of the Uonuma Group．In this area，
some Quatemary fo1dings have been detected geomorpho1ogica1ly without any geo1ogic evidence．
b．ルーo8α〃ゴα’一θα（Fig．3－8）
The Oguni River，a branch of the Mogami River，f1ows west from the backbone range of
northem Honshu（the Oou Mts．）through the town of Funagata．This river crossεs the hi11y1and of
the P1iocene Fumgata Group perpendicularly to its fo1d axes，and has many f1uvia1terraces．The
temce surfaces indicate remarkab1e deformation as shown in the midd1e section of Fig．3・8by
projected promes．The mode of the1ower section，showing the fo1ded structure of the Funagata
Group，is succeeded by the mode of the terrace deformation，and even by that of the present
deformation，which is shown in the upper section based on the repeated1evellings in1954and1964．
From the evidences and estimated years of the terraces，Sugimura（1967）obtained a hypothesis
that the folding started at the beginn血g of the Quatemary and continued to the present with a nearly
constant rate of deformation．
c． τ乃θハた〃一〃1・o1セ〃f〃∫〃伽，θα∫κ〃一17oκκαfdo（Fig．3・9）
The land of the Nemuro Peninsula and its root is an up1ifted abrasion platform，which is
composed of the veneer of the marine Pleistocene，over1ying monoc1ina1Cretaceous strata with
c1inounconformity．The form of the abrasion platform is shown in Fig．3－9by restored contours．
Although there are three temce surfaces of30＿50m，50＿70m，and70＿80m high withindistinct
scarp lines，the whole shape of the platform is of a reversed canoe．North of the abrasion p1atform，
a1ong the Furen River，there is a depressional zone，which is刷1ed by the upper Pleistocene
Nishi・shunbetsu Formation．From these evidences，the p1atform was supposed to show an antic1in創
fo1d㎞g（Kaizuka，1961）．
3．2．3．Regiona1distribution
a．肋卯必〃ゴ0〃0グα〃〃’η01伽θ∫
Fig．3－6，a simp1ified map of No．5，shows the distribution of the anticlina1axes of the
Quatemary fo1ds．The Quatemary fo1ds are distributed densely in northeastem Japan，especia1ly
a1ong the J刮pan Sea coast of Tohoku，whi1e they are sparse in southwestem Japan．When this map is
compared with the map show㎞g the distribution of Neogene and Pleistocene deposits（Fig．3・10），it
must be evident that the distribution of Quatemary fo1ds coincides we11with the distribution of
Neogene and P1eistocene deposits．
This coincidence depends partly on the reason that a great number of Quatemary folds in Fig・
3－6were derived fmm the fo1ded structure of the upper Pliocene and Pleistocene strata．About one
third of the fo1ded axes in Fig．3－6，however，were discovered from deformed marine and nuvia1
terrace surfaces．Therefore，the coincidence depends not on1y upon a superficia1accordance between
the distribution of the source material and that of the derived evidence from the same source，but
a1sO upOn an essentia1reason，i．e．，on the younger and more deformab1e rocks such as the
Neogene・P1aistocene deposits，fo1ding occurs more easi1y than on the o1der and more rigid rocks・This
一42
新
Name ofTem㏄Plain
、ク
ニ1！zε二臆嚇燃詰c、
Direction of Deformation
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’ 」
、4く 1 ヨ “ ’一 ’
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一
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100 50
①
100
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100
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44、
2 4km
耽．3・7． Restored contour map of the fo1ded river terraces and the止cross
sections in Niigata area，Centra1Japan．
一43
十1ド」一一一、一 、150 仏一、一、
1。・妬■L＋J片：1＝：㌃≡三三三｝三㌧。㌦。。。へ。。甘也。。。
50
♂ 一・杣LT
！か！、＼．．．、r
＿。。、．、洲一一…F杜一二三少二 R1、’ER 日FD
O l ＿
〔．］・・1（・Nl
4 5
〔二〕・1・・ヒ・・
6 7 艘 9 10 H I■二 1’バm
Fig．3－8． Profi1es of the terrace surface（midd1e），section of the geo1ogic structure
（1ower），and the present vertical movements of1954－1964（upper）in
Funagata，northwest of Sendai，northem Japan（Sugimura，1967）．
In the midd1e profi1es，vertica1sca1e is exaggerated10times；in the lower
section there is no vertica1exaggeration．
l O km 亀臼
a
1……b
□C
羊
， ．な■ 1、一ギー一・・．．
’ 一 ，
一 I ！ 一 ＼
．、，、
！ ⑪ O
∵／
‘■・。．、
、ノ、；ζ
＿4
一！k」、二
ε8
婁8
0X10
Y O m
20km 20 40 60
Fig．3－9． Restored contour map of the fo1ded coastal terraces and the cross section in
Nem皿o area，eastem Hokkaido（Kaizuka，1961）．
a：Boundary of terrace；b：Lower terrace≡c＝Recent coasta1and al1uvia1p1ain、
一44
2 4
6
4 、／て
2 、 ノ 1 ■ ／ノ 1 ！
■ン 12
・ り2・ 、
’ 、／ 、’ ノ1
4 ・
4’’’’、ノ／’一二 。一 。・ ／ ■ ’ 7ノ／／㌧ 一一ノー
一1。二／4ζ！三・、・
ゑ・
o
◎
68
10／
2
44
1庇一」一・1
0二＝00km
Fig．3・10． Thickness contours of the Neogene and P1eistocene forma－
tionsinJapan（compi1ed byChinzei，1968）I
Contou工interva1：2kmOblique1ines：nothing or very thin layer of the Neogene－
P1eistocene．
will also be supported in the1atter part of this report from other evidences．
b。舳α〃o〃加舳θ〃α舳〃dw砒1θ〃8肋
The mean rate of fo1ding is calcu1ated by dividing O byτ，rbeing the time duration from the
age of the fo1ded terrace surface or fo1ded stratum to the present，and G the gradient of fo1d．The
gradient G is obtained from either of the two equations：G＝2〃／ムor G＝tan x，where〃is wave
height，ムwave1ength，X ang1e of s1ope at a1imb of the fold．
The re1ationship between thus obtained G／r（change of gradient or ve1ocity gradient）andムis
shown in Fig．3・11．This diagram is essentia11y simi1ar to the previous1y presented correlation diagram
for some Japanese and foreign fo1dings（Kaizuka，1967）．Both diagrams indicate that the shorter the
wavelength is，the more rapid is the rate offolding，and also indicate that the increase ofwave height
without any remarkable fau1t seems to have an upper1imit ofabout2mm／year．
一45
／伽ε〃
1000
500
l OO
一｝
〕 50
皇］
0〈叱
oLO」］
o r O
Zく〔
工
O
0ち
㌧ざ1い。浄
6べ
●F
OF ◆
十 F㌔ OF ● △F
十
FFO
◆
O◆へ 十
φφ・O
十8◆◆◆★
… 一
◆X
▲
▲
●Ar O △ △
○A2 ▲▲
◆A3φA一
△
十B
XC▲D△E
O．1 0．5 5 10
WAVE－LENGTH（L）
50 「00km
Fig．3＿11
A1：
A21
A3：
A4：
B：
Re1ation between change of gradient or wave height and wave－
1ength of Quaternary fo1d in Japan．
Nhgata Area C： East Hokkaido
Uetsu Area D： Kanto Area
Ishikari Area E： Kinki Area
Toyama Area F： Accompanied with remarkab1eSouth Fossa－Magna fau1t
Fig．3－11also shows that the chmge of gradient is most1y1ess than10イyear．This value is
much the same with the a㏄umu1ating ratio of horizonta1shear strain，ca1culated from re－triangu1ation
data in the past50＿60years in central and southwestem parts of Japan（Kasahara and Sugimura，
1964）．In Fig．3－11，however，thereexistsarapidmte offolding，more than1o’6／yearinNiigataarea．
c．αo醐ρ〃ω1弥卯沁〃ゴo舳ヅ伽〃陀舳∂ρ〃〃θ7〃岬〃∂肋9〃θω
Fig．3・12shows the distribution of the va1ue G／r Hereby，the regional difference of the rate of
fo1ding is evident，even though the ca1cu1ation ofG／τis only tentative．Based on this fact and a1so on
the regiona1difference in axis・direction（Fig．3・6）and wavelength（Fig．3・11），Kaizuka（1968）
attempted to classify the Quatemary folding areas in Japan as fol1ows一
一46
28I ’32． r36’ i40’
仙’
4o
」H、、。。。。。。。。一。。。
（・1い〕 一L＿．．
o ＜10 1
■ r0－20
舎 20－5C
◆ 50－100
●l00－300
■■［11「L■■■■
■ 、 ■ 口
！ o．l O O・
「 1 ’
一← 一A31
。〆
A2
◆・
！ C’ ．
’→一一’’
■」「
〃
4o．
36’
32．
ノ37
。！ lJ 300べm
「32． 136’ 144’
Fig．3－12． Distribution
Japan．
of the rate（G／T）of Quatem肛y fo1ding in
As indicated in Fig．3－12，the fo11owing areas are c1assiHed provisiona11y（Table3－1）．
The aエeas，A1，A2，A3 and A4，are subdivisions of a nearly continuous fo1d zone，
Ishikari＿Uetsu＿Toyama zone，in which the directions of fo1d axes are concordant with the direction
of the Northem Japan Arc．In Fig．3－11，each fo1d is given with a symbo1ofeach fo1d area．
3．2．4．Disccusi㎝s㎝thefomati㎝o川eQuatem町fo1di㎎sa．肋κoグ〃∂肋8M〃〃肋κ〃∬oグ∫θd肋θ肋ワ70cκ∫
It has been noted that the Quatemary foldings having shorther wavelengths and greater rates
were fomed㎝the thick Neog㎝e or Neog㎝e＿P1eistocene fomations，w㎜e those havi㎎1㎝ger
wavelengths and sm釦1er rates were on o1der and more rigid rocks thanNeogene formations（Kaizuka，
1967）．This regularity may also be found in a comparison ofFig．3－10with Fig．3－12．The thicknesses
of Neogene－Pleistocene fomati㎝s in Fig．3－12are compiled by Chinzei in1968．Quantitatively，a
fo1d of more thm5x1O■7／year in rate is genem11y o㏄urs when the Neogene＿Pleistocene thickness
is more than4km．The exceptions are the Kanto Area and the northem Ishikari Area，where the
Neogene－Pleistocene formations seem to be too thick for such smal1rates offo1ding．
As main factors contro11ing the rate of folding，the fo11owing two may be counted；one is the
一47
Table3・1 Quatemary foldingareas．
Area Strike of axes Wave－le㎎th（km） Rat・（G／T）（1O■＾ノyear） Remarks
A1） Niigata NNE－SSW O．5－5 300－50 the StrOngeSt
fold area in
Japan
Aコ） Uetsu parallel to the Japan O．5－30 100－5 the so－ca1led
Trench（NNE－SSW） Uetsu fold zone
excluding A一
A。） lshikari near1y N－S 1－10 100－10
A。〕 Toyama NE－SW ca1O ca20
B） South concordant with 1－6 100－1O
Fossa－Magna the Sagami㎜dthe Sumga Trench
C） East Hokkaido paral1e1to the Kl1正il 4－20 20－5Arc（ENE－WSW）
D） Kanto nea正1y pa正allel or lO－30 10－1 weak fold in
pe正pendicular to the Neogene一
Sagami Tr㎝ch P1eistocene
formations
E） Kinki nea正1y N－S 1－1O 5－1 weak fold in
Plio－P1eisocene
formations
nature of rocks for tectonic stress，the other is the state of the field of tectonic stress in the crust．The
above－mentioned thickness of Neogene－Pleistocene deposits is concemed with the nature of the
rock．As for the state of the stress fie1d，information on the direction of the maximum compressive
stress in the Quatemary and the present has been increased recently in Japan．
b．Dかεc〃o〃oグ∫b1∂αx’∫α〃d f乃αf oグcoη一ρ’‘θ∫∫かθ∫〃θ∬
From focal mechanism，seismo1ogists have extensively examined the axis of maximum
compressive stress（Honda，1960；Ichikawa，1965）・Fig・3－13shows axes of maximum compressive
stresses at hypocenters of very sha11ow earth（1uakes（earthquakes in the crust）in1927一一1966（Honda
αα五，1967）．It was known that the axes were nearly horizontal．As is shown in Fig．3－13，the
distribution of the directions of axes of max㎞um compressive stress are most1y systematic，namely，
near1y pe11～endicu1ar to the trend ofHonshu in northeastem Japan，and near1y para11el to the trend of
southwestem Japan，except in the South Fossa Magm，繧round Shikoku Is1and and at the Kii
Peninsu1a．Comparing Fig．3・13with Fig．3・6，it is obvious that there exists a c1ose re1ationship
between the directions ofthe fo1d axes and the stress system detected from very sha1low earthquakes．
That is，the pressure direction is a1most perpendicu1ar to the direction of the Quatemary fo1d axis，
even in the above－mentioned exceptiona1Tegions of the South Fossa Magna，Shikoku and Kii．
The distribution of maximum compressive stress in the Quatemary was disc1osed by Matsuda
and Sugimura from the studies of conjugate sets of strike－slip fau1ts in Centra1Japan（Fig・3－14，
reproduction from Matsuda，1967）．Thus the tendency of compressive stress direction in the
Quatemary is in accord with that of the present Centm1Japan shown in Fig．3－13．
Furthermore，Kasahara and Sugimura（1964）pointed out that the direction of the axis of
minimum principa1strain in westem Japan，which was ca1cu1ated from retriangu1ation data of the
past50－60years，is genera1ly in a㏄ord with the compressive axis direction deduced from the focal
mechanism of very sha11ow earthquakes in the same area．
Thus，the above－mentioned four independent evidences，i．e．，state of stress analyzed from
present earthquakes and triangu1ations，Quatemary faults and folds，1ead us to the conclusion that the
－48一
Quatemary fo1dings in Japan seem to be products of the stress system having been active during the
Quatemary and even at present。
132〔 136o 140＾
ベペ
4C
36『
寸
1 1ゲ †
θ
“
〆／
＼」、 ＼＼r
l l
バ＼
！ 44。
40。
36
詞41（
32。
oo 1 ■ ■「I■
＿．＿十一一一一一一一一一一一
0 300km
140。
32。
「3二i 「36o
Fig．3－13． Distribution of the direction of maximum compressive st正ess
disclosed by foca1mechanism of very sha11ow earthquakes
during the period from1927to1966（Hondaαα五，1967）．
3．2．5． References
Hatori，K．，Kaizuka，S．，Namse，Y．，0ta，Y．，Sugimuエa，A．and Yoshikawa，T．（1965）：Quatemary
tectonic map of Japan（a pre1iminary note）．ノ、Gθodα．I∫oc．∫αραη，VoL10，pp．111－115．
Honda，H・（1960）：The genemtion of seismic waves．〃b．1）o閉榊oη0わ∫．，0ttawa，Vo1．24，pp，
329＿334．
，A．MasatsukaandM．Ich此awa，（1967）：Mechanismofearthquakesandstressesproducing
them in Japan and its vicinity（th止d paper）．0εoρ妙∫・〃昭．，Vo1．33，pp．271－279・
Ichikawa，M・（1965）：The mechanism of earthquakes o㏄urring in centra1and southwestem Japan，
and some re1ated prob1ems．肋ρθ7∫加〃αθ0701．αη∂Gεoρ〃．，Vo1．16，pp．104－156．
Ikebe，N．（1942）：Active fo1ding in Echigo oi1fie1d．∫αρ舳λ∬oc、アα．τεoん．，Vo1，1O，pp．184＿185
（in Japanese）．
Kaizuka，S．（1961）：Undulatory crusta1deformation of upper P1eistocene terraces in Japan．Gθogr．
8伽伽∬伽∬．乃〃伽〃α，PP．119－131（肋∫αραη㈹w舳肋飾乃αわJ〃σ剛．
一49
（1967）：Rate of fo1ding in the Quatema町and the present．Gθog7．Rερ．τoκγo〃ε炉oρ．
びη〃．，Vo1．2，PP．1－10．
（1968）：Distribution of Quatema工y fold，especia11y rate and axis direction in Japan．
Gθog7．Rερ．τoκγo〃θ〃oρ．ση加．，No，3，PP．1－9．
，A．Sugimura，Y．0ta，Y．Naruse，T．Yoshikawa and K．Hatori（1967）：Quatemary
tectonicmap ofJapan（thesecondreport）．ρ〃κ閉〃加，Vol．8，pp．289＿295．
Kasahara，K．and A．Sugimura（1964）1Spatia1distribution of horizonta1secua1r strain in Japan．∫
0θo∂α．8oc、∫αρα〃，Vo1．lO pp．139＿145．
Matsuda，T．（1967）：Geology of earthquake．∫．8θ心肌．8oc．∫αραη，Vol．20，No．4，pp，230－235（in
Japanese）．
Ota，Y．（1969）：Crustal movements in the late Quatemary considered from the deformed terrace
plains in north－eastem Japan。∫αρ伽．∫、Gε〇五0θogr．，Vo1．40，Nos．2＿4，pp．41＿61．
0tuka，Y．（1942）：Active rock fo1ding in Japan．〃oc、∫㎜ρ、λω∂、．1αραη，Vo1．17，PP．518－522．
Sugimura，A．（1952）：On the deformation of the earth’s surfaces owing to the rock fo1ding in Japan．
8〃1．Eα〃んg．Rθ∫．1〃〃．，No．30，pp．163－178（肋∫αραηθ∫θw〃ん亙ηg〃ψσb∫卯αα）．
（1967）：Uniform rates and duration period of Quatemary earth movements in Japan。∫
Gθo∫．0∫ακααゆびηル．，Vo1，10，pp．23＿35．
イ ／
∴／、！
∵∵ブ∵∴㌻
∴！ 」Fig．3・14． Distribution of diエection of maximum compressive
stress estimated from active strike－s1ip fau1ts（Matsuda，
1967）．
Light dotted1ine：active stl＝ike－s1ip fau1t
Heavy solid1ine＝1oca1direction of maximum com－
P工essive stress
Heavy broken1ine：genera1direction of maximumcompressive stress．
3．3．Regi㎝a1ch汕acteristics・fQuatermWfault・andfold・
Genera11y speaking，Quatemary fau1ts and folds are more dense1y distributed in regions，where
upper P1iocene formations are extensive1y developed，than in regions composed of formations of the
other ages and igneous rocks．This fact does not represent any regional chamcter of the intensity of
Quatemary tectonic movement，but is a natura1resu1t of the above・mentioned processes of finding
the Quatemary fau1ts and folds．In genera1，faults and folds dislocating P1iocene formations are more
intense than those dis1ocating Quatemary formations and1ess instense than those dis1ocating o1der
formations，because the o1der formations had more frequent1y suffered fau1ting or folding．It is，
50
however，usa11y very difficu1t to ascertain by the above・mentioned method whether or not fau1ts in
o1der formations have been active in the Quatemary．Therefore，in such o1der formations，there are
not so many fau1ts which were definite1y proved with sound evidences of their activity in the
Quatemary，even if they had been active in that age．Consequent1y，Quatemary fau1ts and fo1ds are
more easi五y found by the above method in regions composed ofupper P1iocene formations．
A㏄ording1y，the distribution maps ofQuatemary faults and fo1ds，such as Nos．4and5，do not
seem to fit the present purpose，but it can be considered that these maps are，though not enoughfor，
but necessary for deve1opment of fundamental research on the prediction of earthquake，because it
wi1l not be exprected in near future to compi1e a map w㎞ch contains al1ofQuatemary active fau1ts
and folds．From these considerations，it is concluded that regional characteristics ofcmsta1activities
in the Quatemary may be detected in these maps to some extent，though these maps do not exact1y
represent the intensity of crustal activities in a strict sense．
Quatemary fo1ds are more dense1y distributed in Northeast Japan than in Southwest Japan．
This fact is part1y due to the－extensive distribution of Neogene formations in Northeast Japan，but
main1y it resu1ts from an essentia1relationship of the deve1opment of fo1ding to the distribution of
thick Neogene formations．That is，the development of fo1ded structure is genera11y remarkab1e in
regions composed ofyounger thick formations．
Strikes of fau1ts and axes of folds，一as criteria of infeming the regiona1character of tectonic
activity，are regional1y different．In the westem part of Northeast Japan and Hokuriku District，
strikes of both faults and folds are para11e1to the Honshu is1and arc．0n the other hand，in Centra1
Japan，remarkable faults show strikes trending from ENE to WSW and from NNW to SSE，but such
distinct trends are not found in strikes of folds．In Kinki District，fau1ts trending from NNE to SSW
are predominant，and active strike－s1ip fau1ts are developed a1ong the Median Tectonic Line in Kii and
Shikoku Districts．The strike－s1ip fau1ts deve1oped in Centra1Japan，Kihki，Kii and Shikoku be1ong to
one strain system caused by compressive stress trending E－W．
4．Gipfelf1ur Map
Gipfelflur as defined in this report is a descriptive delineation ofthe earth’s surface，expressed
by a surface touching the highest points of land masses se1ected a㏄ording to certain criteria．The
heights of the Gipfe1nur approx㎞ate1y represent an㎞tegrated sum of crusta1movement and the
1owering of1and surfaces by denudation in the recent geologic time．In such r噌ons as Japan where
crusta1movemeht has been very active in the Quatem趾y，however，the heights of the Gipfe1f1ur are
considered to have been determ㎞ed main1y by recent crusta1movement．
From this point ofview，the Gipfe1nur map is very usefu1to obtain a genera1view oflandforms
and to estimate a ro1e of recent tectonic movement in the geomorphic deve1opment of the Japanese
Is1ands．Fortunate1y，a Gipfe1nur map of1：200，OOO covering entire Japan has a1ready been prepared
by Prof．0kayama in order to clarify the modes of the manifestation of morphogenetic cmsta1
movement as the first step for the morphostructura1devision of the Japanese1s1ands．
As to the regions other than Central Japan，each sheet of topogmphica1maps on a sca1e of
1：50，000（15’in longitude and10’in latitude）was divided into80meshes of1．5’in1ongitude and
1．25’in latitude，and then，the highest point in every mesh was selected．These highest points were
p1otted on topographica1maps of1：200，000and Gipfe1f1ur contour lines were drawn with
interpolation niethod，basing upon their heights．
As to Central Japan，all crests expressed by c1osed contour1ines of isop1eths of every100
meters on topographica1maps of l：50，000were picked up without se1ection，and血e Gipfemur
contour lines were drawn using the heights of these crestes，though some of them were not used
because of their discord㎝ce in height to neighbouring vrests．In some areas such as vo1canoes，fau1t
scarps㎝d so on，convenient methods were used as far as they were considered to be appropriate for
the present purpose．
一51
The original Gipfelflur map of Japan prepared by Prof．0kayama was compiled by himselfinto
three sheets on a scale of1：800，000．The Research Group for Quatemary Tectonic Map synthesized
the three sheets into one sheet on a sca1e of1：1，000，000，and then，Photographical1y reduced it to a
sca1e of1：2，000，000（Map No．6）．In the Gipfe1f1ur maps，original and comp1ied contour lines were
drawn at intewa1s of100meters，but in the Map No．6the contour1ines are drawn at interva1s of200
meterS．
5．Discussi011
5．1．Tect011ic setting of tlle Japanese lslands
5．1．1．Topogmp1lical amd geop11ysica1featmres
Fig．5－1was prepared for mak㎞g a g1ance at the1arge・sc創e topography of island arc systems in
Japan and its environs，on the basis of a map of the Maritime Safety Agency（1952）．Land surface and
seaf1oorshallowerthan2500mareshadedandmountainareashigherthan1500mareblackened．Seafloorsdeeperthan6500marea1sob1ackened，butcanbediscriminatedbyinspectingwhetherthearea is sumounded by a white part or not．The remaining areas ofintermediate depths are1eft b1ank．
’ ’舛イ
，勺■
‘・
・吋1
悩十1500m ・㌔ ●
邊
0一500
●
．90khotskSea
③
・ ’一2500一 ■ 皿 ■50■
一4500 〆
“ 8 劣！ 〆。、似ダ、，
一6500 劣 o ■
一8500
⑰●
●●
●
9・が’． J叩anSea’
りo
‘●
』■40．
oo1 ●
●
（…）
’
‘
o’ ■．
ノ・一 ○”’・ ‘ 、
EastChina． oSea o i
●■ o oo ■・ ●
』
、 E←
8 θ o ∂■●
■目 oo
町㍉． o一 oo θ
■ o，
＾30■
oo
■o
o’6
o o
oo o o‘ 「 『 o
ooo
‘ o o o」■
⑤ ◎ o。．〆ぬ o
oo σ θ oO o・○
団
o、
o0
o； ．。・1。。Ph1llpP
θ．o
● 0So
ineSea’． o o
o o ◎ 〆夢鰹。㍗1㌧ o Q。・．。翰
20一
’‘’
、．○己
穴カプ4
● o‘壮
’ 夕／、
O’’
，堕●
．¢ ■
o ．■■ 軸oo・● ζ
①一
＝＼考、ど靴“撚牢
o
ω桃㎡喝r鷲労・、。 O O’
10．
ζ o‘■ ．一
φ 二綬’、…卿都’8 140． ⑥α
■ ■ 一易
◎o
貞 9◎■
一 o
ooo
四
20一
イo
1；『 160’ 170．
Fig．5・1．Majoτtopo阻aphy of Japan and its environs．
52
Theregionshigherthan－2500mwou1dnear1yrepresentthesurfaceofcontinentallithosphere，
and those of the inte㎜ediate depths（white parts）the surfa㏄ofoceanic1ithosphere．Most ofthe
d・・p・・tp・・t・…th・・・…i・t・㎝・h・…d…th・・ghtt・・・・…p・・dt・th・…f・…f・i・ki・g・・…i．
1ithosphere．
The subsidence of the Japm Trench，amounting to about4000m，is suggested to have taken
p1ace in the Quatemaワperiod．Various sources of evidence may support this proposition．1勾ima and
Kagami（1961）found that a point，now at the2200m depth on the continenta1s1ope west of the
J・p㎝T・…h・w・… th・・h…㎞・i…m・・g・i・th・1・t・P1i・・・・・・・…1yPl・i・t・・・…p・・h．
A㏄ording to Ludwigα〃．（1966），a su㏄ession of step fau1ts that cut the soft sediments as weu as
th・・・…n・・・・・…b・・…“・・gth・J・p・・T・…hbyth…n・・ti・・t・・㎞iq・・．T㎞・f・・t・・g9・・t・
that the process which formed the trench is sti11going on．
口111・1・1・川1・・
㎜・EGA・1VEGR・・lT…0舳・・
囮・OSl・1・E・…1・・・・・・…
皿・醐・1・E・・・…。…。・…
目1111・ll11・・丁・！・川・・…
区ヨVOLC州1・BE・・
■
U≡ ゴ
悌
■
／／／義
’
一 ～、 マ、 込
、 て＼㌻多＝1三
、
△
＆《
．． ．η
θ
倶之
8EL ρ
‘一 ；、・｛、．
～螂 尽1’〃
一、、，、、、孝ジ
ヒ
ム
ψ
＼“：、
、
Fig．5－2． Map of Japan showing island－arc zonality．
teXt．
For symbo1es，see the
一53
The most remarkab1e feature found in Fig．5－1is two pairs of each one is1and arc and one
trench．0ne arc is fo11owed a1ong the westem border of the North Pacific ocean basin，starting from
Kamchatka and extending through the Kuri1es and Northeast Japan to the Izu（Shichito）一Mariana
arc．AnotheT arc extends from Kyushu through the Ryukyu and Taiwan to the Philippines．These two
is1and a正c systems show remarkab1e endogenic features，especial1y active vo1canoes and deep
ea正thqu永e foci，as shown in Fig．5－2．
Fig．5・2shows is1and・arc zona1ity in Japan．The submarine trenches are drawn at depths greater
than6000m（Maritime Safety Agency，1952）；the be1ts of negative gravity anoma1y have△go川≦
＿1OO mga1，and the belts of positive gravity anoma1y△go“≧十100mga1（Sugimura，1960）；the be1ts
・f・・g・ti・・h・・t・n・w…m・1yh・・・・…t・1h・・tΩ・…≦1．0・1O’6・・1・m■2…一1，・・dth・
positive heat－flow anomalies≧2，O x10’6ca1cm■2sec■1（Uyeda and Horai，1964）．The heaW lines
on the eastem edges of the Quatemary vo1canic be1ts represent the vo－canic fronts・The curves
marked with85㎞，155㎞，etc．are iloplethl of the mean hypocentra1position of deep－focul
…thq・・k・・．Th・・・・・・・…p・・…t・・1・・・…d・・i・・df・・m・tmg1y舳i・・m・gm・withθ≦31，th・
t・i・・g1・・th…f・・mw・・k1y・1k・1i・・m・gm・f・・whi・h31＜θ≦36，th・・p…i・・1・・th…f・・m
high・alumina basa1t magma38＜θ≦40，and the c1osed circ1es those from tho1eiite magma with
40＜θ．（Concemingθ，see Sugimum（1968）．）
Northeast Japan is㎜ustraited in Fig．5－2as a typica1is1and arc．Southwest Japan is the
northeastem exitension of the RyOkyO arc，but it1acks typica1is1and・arc features．The Nankai trough
off the Pacific coast of Southwest Japan has the deepest part of about5000m and could not be
ca11ed a trench．Any c1early active vo1cano is not found and any earthquake focus deeper than100
㎞hasnotbeenfoundthere． Consequent1y，the Japanese Is1ands can be divided into active Northeast Japan，very closely
connected with the sinking Pacific Ocean1ithosphere，and inactive Southwest Japan，only indirect1y
related to the endogenic disturbances．
5．1，2．Geo1ogical structure
For convenience ofdescription ofgeo1ogic structure，the main part of the Japanese Islands may
be divided with two1ines：a1ine provisiona1ly ca11ed Sapporo－Tomakomai Line（S－T in Fig．5－3）md
a fau1t called Itoigawa－Shizuoka Line（I－S in Fig．5・3），into three parts：Hokkaido，Northeast Japan
and Southwest Japan．
The westem zone（9，10and11in Fig．5－3）of Northeast Japan is large1y made up of fo1ded late
Cenozoic sediments over1ain by Quatemary vo1canic rocks，and under1ain by Mesozoic and older
rocks which crop out o阯y in p1aces between them．The southem continuation ofit is the intensive1y
deformed area east of the Itoigawa－Shizuoka Line．This area is customari1y called Fossa Ma馴a．The
ltoigawa－Shizuoka fau1．crosses and cuts the structure of Southwest Japan，which was formed prior
to ear1y Miocene and reappears beyond Fossa Ma即a in some parts of Northeast Japan．
In the westem zone of Northeast Japan and its extensions to the south to the Izu－MaTiana arc
and to the northeast to the Kuri1e arc，a series of orogenic events started at the beginning of the
Miocene epoch．The trend of the1ate Cenozoic orogenic be1t is discordant with those of Mesozoic
orogenic belts．The younger orogeny seems to be genetically independent of the o1der ones，a1though
the older structures have given some effects on the younger ones in Central Hokkaido and in southem
Fossa Magna．The Mesozoic and o1der orgenic be1s are distributed in the eastem zone ofNortheast
Japan，Southwest Japan，and Hokkaido．
The eastem zone of Northeast Japan consists of Kitakami Plateau，Abukuma P1ateau，Kanto
Range，and some other ranges．Pa1eogene and older rocks are distributed in these areas．
Southwest Japan is divided by the Median Tectonic Line（MTL in Fig．5－3），which trends
a1most east－west，into two zones：i．e．，the Outer Zone and the lnner Zone．The Median Tectonic
Line has1ong been thought to be a thrust with which the Inner Zone overlies the Outer Zone，but the
need of re－examination is arising because it was found recent1y that there occurred a right－lateral fault
一54
at1east during Quatemary period（0kada，1968）．The westem extension of this fau1t to Kyushu is
made obscure by the cover ofCenozoic sediments and volcanic rocks．
The lnner Zone of the Southwest Japan comists of Pa1eozoic and Mesozoic sedimentary and
metamorphic rocks as we11as plutonic rocks intruding them，covered with Cenozoic sediments（4，5，
6，7，and8in Fig．5・3）．In the Outer Zone，there is an east・west trending zona1arrangement of
tectonic provinces，in which the southemmost one is ca11ed Shimanto be1t，The Shimanto belt
consists1argely of non・fossi1iferous and part1y fossiliferous Mesozoic and Pa1eogene sediments and is
overlain unconformab1y by Neogene sediments（1and2in Fig．5・3）．
Hokkaido contains a be1t of metamorphic rocks cal1ed Hidaka orogenic be1t in its midd1e area in
a norther1y direction pointing Sakha1in．A be1t of deformed Jurassic strata with granitic and ultrabasic
intrusives makes up the main part of the be1t．A fold be1t ofCretaceous，Pa1eogene and Miocene strata
（12in Fig．5・3）is on the west next to the north－south trending metamorphic be1t．
Down－fau1ted or down－warped basins，scattered over the Japanese1slands，trap the Quatemary
System，which forms p1ains and neighboring terraces and hi11s．Kanto Plain is the1argest of these
basins（3in Fig．5－3）．
132 136 140
44
O’ 12・◎
4
S ■ ■
011・ 、 ■
θ T
40 o
、ポi。．S∀ KlTAKAMI、
ざ
ダ 島 、．1。θθ・・・・…
1 ら令36
32
6．一7．一 “ “O。． 、
8 ・・3 s。。．．搬
Fig．5・3－Distribution of Cenozoic formations in Japan，with
divisions ofNeogene provinces（Ikebe and Chiji，1969）．
For I－S，S－T，MTL and numbers，see the text．
55
5．1．3．Referellces
呵ima，A．，and Kagami，H・（1961）：Cainozoic tectonic deve1opment of the continenta1s1ope．∫．Gθoム
∫oc。．1αρα〃，Vo1．67，pp，561＿577（加〃ραηθκw｛肋万η8〃曲α肋〃oα）．
Ikebe，N．，and Chiji，M。（1969）：Neogene biostrati町aphy and geochrono1ogy in Japan．8〃zεη∫〃一
Kε〃κγ〃，0ccωゴo〃〃肋ρθ岬介o榊肋θ0〃肋〃「“κ〃㎜o1〃α伽〃1〃肘γoγ，Vo1－1，No．4，pp．
25＿34．
Ludwig，W．J。，Ewing，J．I．，Murauchi，S、，Den，N．，Asano，S．，Hotta，H．，Hayakawa，M．，1chikawa，K．，
and Noguchi，I・（1966）：Sediments and structure of the Japan Trench．．1．Gθoρ妙∫．Rθ∫、，Vo1．
71．pp．2121＿2137．
Maritime Safety Agency（1952）：Depth Cume Chart of the Adjacent Seas of Japan，Chart No．6901．
Maritime Sefety Agency，Tokyo．
Okada，A．（1968）：Strike・s1ip fau1ting of1ate Quatemary a1ong the Median Dis1ocation Line in the
sunoundings of Awa－Ikeda，northeastem Shikoku．ρ吻比川．Rθκ〃c乃，Vo1．7，pp．15＿26（肋
∫αρα舳θw舳肋81舳αあ鮒〃）．
Sugimura，A・（1960）：Zona1arrangement of some geophysica1and petro1ogical features in Japan and
its envilrOns．∫．ハσc．．∫c’．，ση〃。τoκγo，Sec．2，Vo1．12，pp．133＿153．
（1968）：Spatia1re1ations of basa1tic magmas in is1and arcs．In：H．H．Hess and A．
Po1dervaart（Editors）：Basa1ts，the Po1dervaart Treatise on Rocks of Basa1tic Composition；
1nterscience Publishers，New York，Vo1．2，pp．537＿571．
Uyeda，S．，and Horai，K．（1964）：Terrestrial heat f1ow in Japan．．1．Gθoρ乃ハ．Res．，Vo1．69，pp．
2121＿2141，
5．2．Compads011with Neogeme tectonic movements
The late Cenozoic orogeny in the Japanese Is1ands was summarized by Matsudaαα五（1967），
together with tectonic maps since the Miocene．
Using these maps and the Quatemary Tectonic Maps，Kaizuka and Murata（I969）constructed
tectonic maps of Japan during the Neogene（from the beginning ofMiocene to the end ofPliocene），
and compared the crusta1movements during the Neogene with those of the Quatemary．In the
fo11owing a part of their paper is transcribed with some changes in expressioη．
5．2．1．Vertica1disp1a㏄mellt
Fig．5－4is a distribution map of vertica1disp1acement since the begiming of the Miocene
（Matsudaασ五，1967）．The tota1amount of vertica1disp1acement was assumed to be represented by
the present height of the basal unconfomity ofmarine Miocene deposits．
In the Fig－5－5，the distribution of vertica1disp1acement during the who1e Quatemary is
reproduced from the Quatemary Tectonic Map No．3．
Fig．5－6is a new1y obtained map derived from Figs．5－4and5－5．This shows the vertica1
disp1acement during the Neogene．The procedure for making t㎞s isopleth map was as fol1ows：Figs．
54and5－5were over1apped，and differences ofthe two isopleths were measured at each intersecting
point・then isop1eths were drawn．Thus Fig．．5・6is on1y a rough apProximation for the vertica1
disp1acement during the Neogene．
Throu凶compaTson between Figs．5－5and5－6，the fo11owings are indicated：（1）Du正ing about
25mi11ion years of the Neogene，up1ift of Southwest Japm was very sm創1，especia11y in the Inner
Zone，whi1e during about2mmion years of the Quatemaワ，up1ift of the same region was much
greater and more rapid than in the Neogene．（2）During the Neogene，Northeast Japan subsided as a
who1e，especial1y in the fo皿owing regions：Japan Sea coast of Northeast Honshu，Southem Fossa
Magna，in the centra1part of which Mt．Fuji is situated today，md both sides of the Hidaka Range in
central Hokkaido，On the contrary，duhng the Quatema取，Northeast Japan was up1ifted extensive1y
except in the Kanto，Niigata，and Ishikari areas．（3）Thus，the remarkab1e contmst in vertic創
disp1a㏄ment between Northeast Japan and Southwest Japan during the Neogene disappeared most1y
in the QuatemaW Period．
一56
1川口jm
O
・一101㎜
1 一 一
一1｛UUo
■ 一5000
モ q
ψ、・’
ノ鰯 o
／
仰．ぷ
oo
¢ク
ぢ ’一 ！ ！ II 。’ 、’ノ
！ 1 ㍗
u 川1， ！1＾」km
Fig．5－4． Vertica1disp1acement since the Miocene（Matsuda，Nakamura and
Sugimura，1967）．
The origin of these major characteristics in the1ate Cenozoic orogeny of Japan must be
exp1ained in the future．
5．2．2．Fo1d㎞gordefomati㎝ofstmta
Fig．5・7shows the distribution of a degree of deformation since the Miocene a㏄ording t0
Matsudaα〃．（1967）．The degree of deformation was ca1cu1ated from geo1ogica1sections ofNeogene
rocks，and it was defined asΣ△〃μ，whereΣ4〃is the sum of the vertica1component of fo1ded
Neogene strata and the throw of faulting，andムthe1ength of the geo1ogica1section．
In order to compare with Fig．5－7，Fig．5－8showing the degree of deformation during the
Quatemarywas constmcted from the data of Quatemary fo1dings（ApPendix4）．The deg正ee of
deformation in the who1e Quatemary i§ca1cu1ated by the fol1owing equation：
ΣA〃μ（during the Quatemaワ）：R x2mmion，
一57
15川1m
l l口m
51m
o
－51＾〕
罫m川〕
タ、．！1
〃
ρ 口揃 井㈱6
06ク印
L＿」⊥＿＿」一コー』n1
lFig．5－5． Vertica1 disp1acement during the
Quatemary Tectonic Map，1969）．
Quatemary （Research Group for
where R is the mteofdefo㎜ati㎝orthevelocitygradientpresentedin Appendix4．Thisequationis
based on an assumption that the rate of the degree in Fig．5・7is essentia1ly the same as that of the
I＝ate of Quaternary fo1ding PI＝esented in Fig．5－10．
As shown in Fig．5－8，the degree of deformation is g了eatest a1ong the Japan Sea coast of
Northeast Japan，in the“Uetsu Fo1ded Zone”．0n the other hand，in Fig．5－7three deformed zones
are recognized outside the Uetsu Fo1ded Zone and the Southem Fossa Magna．The three zones are
Ishikari（centm1Hoddaido），Japan Sea coast of Southwest Honshu，and Paci丘c coasta1zone of
Southwest Japan，where a1most no fo1ded Quatemary strata or geomorphic surfaces have been
discovered as yet．Therefore，as mentioned by Otuka（1939），deformationa1process of these zones
had mostly been comp1eted before the Quatemary．
From Figs．5－7and5－8，the map in Fig．5－9showing the degree of deformation during the
58
｝一1川川 1 一 ’
一 一1州πi 1 1一一一 ’ 一
顯 一｝舳〕
・o＝ 〇 一
ゴ，／∵j
〆η・一伽 ■J ウ
排s
刊』伽 一帥
．1㌶」
ち ■”㎜
」灼 1
影
Fig．5－6． Vertical displacement during the Neogene．
Neogene is obtained．Because on1y a sm訓1amount of data was taken from the same1oca1ities in Figs．
5－7and5－8，the ca1cu1ated va1ues of Fig．5・9are taken most1y fromva1ues ofthe nearest1oca1ities in
both figures．Therefore，this map indicates only a rough sketch of the Neogene deformation．
In Fig．5－9，a pecu1iarity is noted in the Uetsu Fo1ded Zone，especiauy on its westem side，
where minus va1ues predomimte．This means that the deformation since the Miocene is1ess than that
during the Quatemary．T㎞s discrepancy may have occurred because of the fo11owing reason：To
ca1cu1ate the degree of deformation in the Quatemary，R x2mi11ion was used，b争sed on the
assumption that the rate of deformation was uniform throughout the who1e Quatemary・T㎞s
assumption is probab1y not correct㎞the region concemed，and it seems probab1e that the
deformation began after the beginning of Quatemary（2m㎜ion yea工s ago），or that the rate of
deformation was accelerated at the end of Quatemary．
一59一
・02
○く・
1、 ！ 1、 ／
θ
一04●
一06●
’08 ◎
’1．O ●
｝3－O
02
〃 ●
o．’
／ ⑫θ
③oθ
θ
留
’02
〇一’ 02 0 ／ 1 ！ 〇一 〇
●
O ／
〃
ノ、1。岨、
／
O 1一〇！／ ！
バ
u 1O0 200km
Fig．5－7． Degree of deformation since the Miocene（Matsuda，Nakamura，and Sugimura，
1967）．
5．2．3．Re1ief
Fig．5－10shows the present genera1re1ief of the Japanese1s1ands．This is a simp1ified map from
the Gipfelf1ur of Japan（Quatemary Tectonic Map，No．6）．Based on this map and Fig．5－5，Fig．5－11
is newly obtained，which presents the relief of Japan at the end of Tertiary．The procedure for
making this map is the same as in the case of Fig．5－6．It is a matter of course that Quatemaw
vo1canoes make no mountain in Fig．5・11．Genera11y，the re1ief at the end ofTertiary is about half or
even a quarter of the present re1ief．Low relief topography of the Japanese Is1mds at the end of
Tertiaワhas been considered so far from evidences that there are the so－called“penep1ain remants”of
the1ate Tertiary in many regions and that facies of Pliocene strata indicate low relief environments．
5．2．4．Comc1㎜si011ahem肛ks
Looking over the maps presented above，it is noted that the character of Quatema町crusta1
一60
o．2
θ
③
●
0
●
O．4
0．6
0．8
1．O
．3．（一
●㊥
●
〃
㊥
○
ま
O O0
4・θ
蛎 o lon ！川〕㎞1
Fig．5－8． Degree of fo1ding during the Quatemary．
movements in Japan are much different from those of the Neogene．In Northeast Japan，■subsidence
which predominated during the Neogene，was rep1aced by up1ifting in the Quatemary，a㏄ompanied
by strong deformation ofNeogene and Quatemary strata．In Southwest Japan，no remarkab1e vertica1
movements and fo1dings appeared during the Neogene，except for foldings of coasta1be1ts of the
Japan Sea and the Pacific．But the Quatemary vertica1movements were not so different from those of
Northeast Japan．
In other words，during the Neogene，the difference was very great between Northeast and
Southwest Japan in the character of cursta1movement．During the Quatemary，however，the
difference was smal1，and near1y the same re1ief making movements took place in the entire Japanese
Is1ands．
5．2．5． References
Kaizuka，S．（1967）：Rate of fo1ding in the Quatemary and the present．0θogγ．Rερ．τoκγo〃θ〃oρ．
61一
0
！＿、 1
→。 θ
1｛＜一！．u
1讐 一 1、‘1一 一 』．1］ 1
＋…］・4 1
一■“’！ ←O・ ＼θ．．、。 ＼ 十。1
●l l．1 ｛ 1
・1－ 4／／／
＼
ズ㍗O O￥一
鰐
Fig．5－9． Degエee of deformation during the Neogene．
σηル．，No．2，pp．1＿10．
一S （1968） Dlstr1but1on of Quaternary fo1d，espec1a11y rate and ax1s d皿ect1on m Japan
Gθog7．Rθρ．τoりo〃θ〃oρ．σηル．，No．3，PP．1－g．
and Murata，A．（1969）：The amount of cmsta1movements during the Neogene and the
Quatemary in Japan．0εo皿．Rθρ．τoκγo〃ε〃oρ．σηル．，No．4，PP．1－10．
Matsuda，T．，Nakamura，K．，and Sugimura，A．（1967）1Late Cenozoic orogeny in Japan． τθαo〃oρ乃ハた∫，Vo1．4，pp．349＿366．
Otuka，Y．（1939）：Tertiary αusta1deformations in Japan with short remarks on Tertiary
Pa1eogeography．J〃わ肌1㍉あ．Co〃！〃一．Pγo∫〃．γ二48亙な60’乃。8かf乃∂．，PP．481－519．
Research Group for Quatemary Tectonic Map（1968）：Quatema町Tectonic Map of Japan． τ加 ρ〃〃θ閉、Rθ∫ωκ乃，Vo1．7，pp．182＿187（加Jαρ伽θ∫θwゴ肋亙〃g伽乃肋∫”αα）．
5．3．Comparison w舳present seismic e11ergy砧stdbutiom
5．3．1．1ntroductio皿
Recent studies have revea1ed that in Japanese Is1and Arc there occurs frequent1y the crusta1
movement a㏄ompanied by great earthquakes of the present age in a1most the same manner as the
crusta1movement in Quatemary，and that in many cases quantitative1y a1so the1atter is near1y equa1
to the integrated sum of the former（for examp1e，Yoshikawaα〃，1964）．This indicates that a fair1y
1arge part ofthe crusta1defomati㎝s in Quatema取mayhavebeencausedbythecrusta1movement
一62
景雌だ
言o
．炉．
．3αX〕m
。o
o
o
o
δ．
2500
．以㎜
6
ピ ・o ・’
矧
、・宇．
1駄刀
1α刀
500
－ o
μ。句．。
8
多
○吋． ・カo d
o loo 以㎜km
Fig．5－10． Re1ief at the present．
a㏄ompanied with great earthquakes．Therefore，in order to know the mutua1re1ations of these
circumstances，study has been made on the status of the re1ease of seismic energy in Japanese Is1and
Arc in the historic age．
5．3．2．Method
As the scientific observation of earthquake has its history less thm100years，the study on the
seismic activity throughout the historic period is compe11ed to re1y on ancient manuscripts．
Fortunate1y，a Japanese year－book“Rika Nempyo”（Chronologic刮Tab1es of Natura1Sciences）
contains tab1es by which we can know the epicenters and sca1es of principa1earthquakes that had
caused臣eater damage in the historic period，and a㏄ording to this year・book the re1eased energy of
such earthquakes was ca1cu1ated．
0n the“Chrono1ogica1Tab1e of Greater Earthquakes in Japan and its Adjacent Regions”of the
1970edition of the above year－book，there are described519earthquakes during the1369years from
一63
1齪加j nl
11＾πi
引πj
2舳 4
o
（1
。、ノ 1
’’ 、 ’ ／、 1 ㌧一 ／ 、 1 ’1い■
り ・J
。ク
州
16’’㌣、
’ ’’、
ノ 11
一7メξ：一、
一二〃一・…4
）多 D’
、．O、＝
／3蛎一／（三
㌔ 、ψ、
、ノ6）
ll lOll ！川1km
Fig．5・11． Re1ief at the end of the Tertiary．
99to1968A．D．0ut of the519earthquakes，167are either ea工thquakes ofu血㎞ownmagnitude or
earthquakes in regions of Korea，Fomosa and Okimwa．Besides，it is considered that a1arge number
of earthquakes of which the magnitudes are less than ca．6were omitted in the description of the
Tab1e．Therefore，excepting 35 eartuquakes with their magnitudes less than5．9and the
above－mentioned i67，the re1eased energy was ca1cu1ated by the fo11owing equation：
1g9亙＝1．5〃十11．8，
where E is re1eased energy，and〃the magnitude．
As these earthquakes o㏄urred on1and and in sea areas within250km from the coast，the a爬a
of epicentra1distribution is divided into meshes ofeach0．ゴin1atitude and1ongitude（767meshes），
md the sum of re1eased energy is ca1cu1ated for each of the meshes．The distribution and the
frequency of the sums are shown in Fig．5－12and Tab1e5－1．
一64
耐1。ぴ1・プ1〃1岨’w■
o■1…町・麗1・”
『ll・■
1 ・
目mH皿m－1 ．42。
口1バ ■ ，
口・1・一〇
二．40。
■
132． 13ぺ 13げ38。
十一→一
128， 130。十十、讐＿
■ ↓γ、七．一，、 ■ ■ ■」．1． 一｝■丁■、■1上鴫
3ぺ
■■
3プ
㍗汁O 500km
■プ、ゴニ
oo古
Fig． 5－12．
、50．14げ 14び
必。
28
Distribution of re1eased energy by earthquakes in the historic
peIiod（O．5 meshes）．
Table5－1 Distributionoffrequenciesofmagnitudesofre1eased energyinthehistoric
period（from Fig．5－12）．
Order of l025・・g・
1024・・g・
1023・・g・
1022・・g・
l021・・g・
l020・・g…d1…
NoI1e of mesh
17meshes34meshes58meshes
24ホmeshes634meshes
＊ As the earthquakes of M≧6we正e adopted，the numbe正is smau．
M＝5are also adopted，the mmbe正is1a－ger。
But if those of t11e011der of
According to Fig．5－12，the maximum is5．9x1024ergs in the neighborhood of Shionomisaki，
and otherwise，sums of more than5x1024ergs are found in the offings of Smriku，Omaezaki md
Shirahama（Kii），and p1aces of the order of1024ergs are distributed continuous1y in the coasta1areas
on the Pacific Ocean side．The va1ue of5x l024ergs corresponds to an earthquake ofthe magnitude
of about8．75，and it is noteworthy that the utmost maximum of re1eased energy even in the pehod
of a thousand and several hundreds years is of such a value．0n the coast of the Jap…m Sea，the
damage is not1ess than on the Pacific Ocean side，but the maximum re1eased energy is4x1023（ne酊
Mt．Hakusan），and it is remarkab1e that the va1ues are1021～1022ergs at most p1aces」n addition，a
conspicuous maximum in the in1and regions is1023～1024ergs in the vicini奴of Lake Biwa．
65
Areas of sma11er amounts of the re1eased energy are found in the in1and part of Hokkaido，in
Kitakami Mountains in areas of Yamagata Pref一，in Abukima Mountains，in Ibaraki Pref．，on the
borders of Gunma and Niigata Prefectures，in Kanto Momtains，in the in1and parts of Shikoku and
Kyushu，etc．
By the way，conceming this distribution map，we must take account of the following facts：（1）
that because ancient manuscripts were the source of this map，there was some unfaimess such as more
detai1eddescriptionoftl1eneighborhoodsofadn1inistrativecenters；（2）thatthe・earenotdescribed
such earthquakes as have caused rather light damage in spite of their1arge sca1es；and（3）that the
assumption of hypocentral positions and sca1es can be erroneous，etc、㎞particular，it is considered
that Hokkaido cannot be compared in the same rank with other regions becuase of extreme scantiness
of the data，
Next，comparison of this energy distribution map with Quatemary Tectonic Map does not
clearly reveal any correlation as is mentioned above．The reasons for this may be，other than the said
problematic points，additionally shown as follows：（1）The absence of the corre1ation may have
connection with the fact that the1ength of the historic period is less than 1／1000of the period of
the Quaternary，and this fact seems to be proved by the resu1t ofour study that the tota1sum of
re1eased energy even in the area of maximum release is corresponding to that of only one earthquake
of the1argest sca1e．（2）Another reason1ies on the side of the Quatemary Tectonic Map・Name1y，the
situations of crusta1movement under the sea surface，vo1canic products and plain deposits can hard1y
be grasped，and so the precision ofinvestigati㎝camot bemifom㎝suchsurfaces．F耐her，as the
data for preparation of the maps were obtained by co11ection of existing research materia1s，the
ununiformity of the precision may have been caused by such circumstances．As for the Quatemary
Tectonic Map itse1f，the maps should be rather regarded as tota1ized maps which show rough1y the
properties of certain areas of some extension than used for finding out the correspondence in detai1．
Therefore，merely aiming at the districts including land，Fig．5－12isredrawnintopartial maps
with meshes of each 1o（Fig．5－13），and these are compared for knowing the distribution and
amounts of uplifts，subsidences，faults and folds．The quadrangle of each l．is110km1ong in
north－south direction and about80一一一95km wide in east・west direction，and the size of this
quadrangle seems to be too1arge for representing the topogmphic characteristics，but general
tendencies on the whole are easier to see by this．Further，by the use of large正meshes，the inf1uences
of sea areas，vo1canoes，p1ains，etc．become largely apparent，and properly speaking，such influences
ought to be excluded，but as the methods of compensation are not clearly known，so the comparison
h劃s been made without any exclusion－
5．3．3．Comparison
On comp1eting such arrangements，we can see．in regard to seismic activity，a be1t of
1024～1025ergs from the Boso Peninsula to Shikiku Island，and another be1t o〔023ergs from Akita
Pref．to Tottori Pref．along the Japan Sea coast．Special1y noticeab1e is the existence of the areas of
1023～1024ergs in the land regions around To吋o and from Gifu Perf．to Kyoto，Osaka and Kobe．
Besides，meshes of1023ergs are a1so seen in the vicinity of Hiroshima．The re1ation between these
and crustal movement is as follows．
First，as for faults and folds，the density of their distribution was taken as indices of crustal
movement．The distribution density is indicated by various methods，but the density was represented
with the number of lines of fau1t or fold within a mesh．1n the case of fau1t，a falut line extending to
another mesh was also counted as1．In the case of fo1d，the number of the set of an anticline and a
syncline was counted as l，but in the case where either of the both was a fraction or missing，then
a1so the number was counted as1．The number of fau1t or fo1d having its extension ofmore than50
km was a1so listed together．In the case of a fau1t with its extension of50km，according to Iida’s
formula：〃＝3．1＋0，631og Z，the fault corresponds to what was caused by an earthquake of〃＝7・3
approximately．Such faults were particularly counted，because they were considered to give some
一66
criteria，if they were to be activated on the occasions ofgreat earthquakes in the past．
Comparison of the map of fault distribution density（Fig．5－14）with Fig，5－13（in this
comparison there are exc1uded the meshes for Hokkaido and is1ands on1y，and the same in the
fonowing）revea1s that the areas，where there are many fau1ts and the energy re1eased by earthquakes
is of the order of1024ergs are the southem part of Akita Pref．，zones of Kanazawa－Lake
Biwa＿Osaka and Kobe，Boso Peninsu1a＿Tokyo and Shonan，and the northem part of Nagano
Prefecture．0n the other hand，the area with a1arge quantity of re1eased energy and with sma11er
densities of faults is Ibara㎞Prefecture．Loca1ities having1ower seismic energy and sma11er fau1t
density are the Sh㎞okita Peninsu1a and the centra1part of Shikoku．Furthermore，the comparatively
high fault density in Kitakami Mountains and Abukuma Mountains are owing to the fact that the
meshes inc1ude even the areas adjacent to the westem part of the mountains．On the who1e，most of
the areas other than the above－mentioned剋so indicate a comparative1y positive comespondence
between seismic energy and fau1t density．A statistica1review of the re1ation between the quantity of
re1eased energy and the fau1t density（Table5－2，the meshes for Hokkaido or is1ands on1y being
exc1uded，the same in the fouowing）indicates that the meshes ofmore than1022ergscontain more
numbers of fault，and especia11y such a mesh as contains two or three1ines of fau1ts ofmore than50
㎞i1notoblervedinalea1of1owenergy．However，thilfeatureilnotveryoftenleeninthearealof1024～1025・・g・，・・dthi・f・・ti・・…id…dt・b・1・・g・1y・ff・・t・dbyth・・it・・ti・・th・tth。。。。。。
where such meshes are distributed are mainly1ocated on the coast of the Pacific Ocean and inc1ude
pretty many sga areas．
As for folds（Fig．5－15），areas with high distribution density of folds and with meshes of
re1eased energy of the order of1024ergs are region of Tokyo－Shonan，the southem part of Akita
Pref．，the neighborhood of Osaka and Kobe，and the northem part of Nagano Pref．：in the high
energy zones on the coast of the Pacific Ocean the density of fo1ds is sm』1as we11as that of fau1t．
Low energy areas are the Shimokita Peninsula，Kitakami Mountains，Abukuma Mountains－Ibara㎞
Pref．，and the centra1part of Shikoku；in these areas there are good agreements．Though the area of
Lake Biwa is a high energy area，there is shown reversed correspondence．Due to the sm汕number of
1i・…ff・1d・，th・・・・…p・・d・…t・th…1・…d・…gyi・th・f・1di…t・・g・・d・・i・th・f・・lt．1・
regard to the frequency distribution of energy quantity and the number of lines a1so，simi1ar
tendencies are seen in fau1ts and fo1ds（Table5－2）．Regarding both offault and fold，the detection is
difficu1t in places other than where there are distibuted the formations younger than Pliocene，and
this dimculty also makes worse the correspondence to the energy re1eased by earthquakes．
For the amounts of upHfted and subsidence，vertica1disp1acements compi工ed耐om the Maps
Nos－1and2（and the Quatemary Tectonic Map No，3）were used，and the amounts of from the
subsidences1argerthan1000mtotheup1ifts1argerthan1500mweredividedinto10ranks，respectively numbered with figures of1to10，as indices．Name1y，the1argest quantity ofupli肚in a
mesh was taken as uplift amount in the mesh，the maximum subsidence simi1arly as subsidence
㎝ount of the med1，and the difference between the both amounts as㎞dex number of gradient．
Thus，simiarly to the case of fau1ts，a map of vertica1disp1acement distribution（Figs．5－16，5－17and
5－18）and a tab1e of corre1ation with energy（Table5－3）are obtained．
Apparent1y，the above－mentioned maps may give㎝impression different from that of usu創
distirubtion maps of fua』ts and folds．First，as to the uplift amounts，Fig．5－16shows that the areas，
where the ranks over9，mmely the up1ift amounts over1000m，are seen and there is obsewed the
agreement with the order of1024ergs of re1eased energy，are the reas near Lake Biwa and near
Muroto．Agreement with the order of1023ergs of energy is a1so found in the northem part of
Nagano Pref。，near Kanazawa，near Osaka and Kobe．0n the other hand，the veW opposite tendency is
seen on the Pacific coast，near Tokyo and near Hiro㎞ima．The correspondence of low energy area
with low－rank1oca1ity is very good in the Sh㎞okita Pen㎞sula，Kitakami Mountains，and Ibarald
P・・f・・t・…b・ti・th・…t・・lp・・t・fShik・k・，・t・．，th…i・・b・・…dth・p・・f・・t1y・pP・・it・
一67
Table5－2． Relation between frequencies of the densities
of fau1ts and folds and the magnitude of re－
1eased energy by earthquakes
EneIgy Fault Fo1d
E正g 1020 1021 1022 1023 1024 1020 1021 1022 1023 1024
Frequ㎝cy
O 3 1 3 1 5 7 10 7 3＊
1 1 1 1 3 3‡ 1 1 2
2 2 2 2 1 1 2
3 1（1） 2（1） 2 1 1 1
4 3（1） 1 1 1
5 1 2（1） 2 2
6 1 1 2
7 2（2） 2 2（2） 1
8 1（1）
9 1（1） 2（2－1
10 1
11 112 1（1） 113 1（1） 1
16 117 1（2－1
25 1
27 1（3－1
many 1
Tota1 8（3） 8（2） 165（2．1 152（3．1 8＊ 8 8 16 15 8＊
Mean 3．O 6．8 5．6 6．6 3．5 O．6 O．5 2．4 2．1 2．O
Rema正ks：
（ ）
（2一）
（3一）
i・・1・di・g・・・…f1025・・g・；
numbe正of meshes inc1uding1line with刮n extension oveI50km；
number of meshes inc1uding2of such1ines；
number ofmeshes inc1uding3ofsuch1ines．
68
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一日
寸Noo oo 一一o 一 寸1
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o o 一【 一NN一 寸〉1
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H＃ キ
一 ㈹一N一oo 〔
o吻……εo
一 oo日
寸N寸門一い ト
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一』〔N寸寸 o 卜o一 一 【
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69
correspondence．Considering the re1eation of the ranking numbers to the amounts of re1eased energy
（Tab1e5・3），the up1ifts of ranks≧9，namely more than1000m occur beginning with the order of
1022ergs，but without any appeamnce of conspicuous features．In consideration of the relation with
the amounts of subsidence（Fig．5－17），areas where the va1ues of1023～1024ergs of released energy
correspond to rank2or l of subsidence amount are the Boso Peninsu1a一一Tokyo－Shonan，and area
on the north of Tokyo，and Osaka and Kobe；the correspondence to1ow energy areas is found in the
Shimo㎞ta Pen㎞su1a，Kitakami Mountains，and the centra1part of Shikoku；and in the areas of1021
ergs a1so there is seen good correspondence on the who1e．On investigating the relatiionof theranking
numbers of vertica1disp1acement to the re1eased energy amount（Tab1e5－3），the areas of subsidence
（1ess than O m）are a11areas of re1eased energy1arger than1022ergs，exc1uding only one example，and
there is observed血e co皿e1ation larger than in the case of up1ift amount．As for the gradient，the
areas of high energy and large gradient（ranks≧7）are the district ofTokyo and Shonan and that of
Osaka and Kobe，but low energy areas have1ow gradients．The relation between the gradient
frequency and the released energy amount（Tab1e5－3）has a tendency that the rank is high in meshes
of released energy1arger than1022ergs．As is mentioned in the above discussion，the corre1ation
between the amount of vertical displacement in the crust and ule amount of energy re1eased by
seismic activity is considered to be not so clear as was expected．Various reasons may be considered
for this，but the regions including sea areas are cal1ed into question．Around the Japanese Is1and Arcs
there are deve1oped such submarine topographies of large depth or gradient as camot be explained
without assuming them to be origi皿ated by the crusta1movement．At such1oca』ities there have
fre’quent1y occur1＝ed great ea1＝thquakes a1so．
The amount of subsidene as we11as the water depth shows comparative1y good correlation with
the re1eased energy from the ground surface on d1e Pacific coast west of the Boso Peninsu1a（Fig．
5－19）．It goes we11for the gradient of subsidence，too（Fig．5－20）。However，the correspondence to the
localities of high energy in other coastal areas is not satisfactory．
5．3．4．Conclusion
As is shown above，the corre1ation of the elements of the crusta1movement with the amount of
released energy by earthquakes in the historic period is not so1arge．Namely，comparative1y good
agreements are observed in areas of Tokyo－Shomn and Osaka－Kobe（in regard to faults，folds，
㎝ount ofmaximum up1ift，amount ofmaximum subsidence，and gradient），in Kanazawa district早nd
the vicinity of Lake Biwa（for faults and quantity of maximum up1ift），and in the Boso Peninsula（for
faults，amount of maximum upheava1，and corrected gradient）．Excepting these and otller severa1
examples，at many of the high－energy1oca1ities the agreement is not so good，Out of such areas，the
Paci丘c coast west of the Boso Peninsu1a w㎜become to have good agreement，if the depth of the
trench be regarded as crusta1subsidence，but in other areas it is not so．
There are areas where the crusta1movement is comparatively1arge，but the energy re1eased by
earthquakes rather low，for example the Hida district．This seems to suggest that in the Hida district
the active periods of Atotsugawa fau1t and Atera f刮ult were longer than the historic time．Besides，
conceming1ow energy areas also there are cases of agreement and disagreement．For the purpose of
earthquake prediction，studies in these respects shou1d be more and moIe promoted．
5．3．5．Refe1－ences
Yoshikawaαα1．（1964）：Crustal movement in the Quatemary revea1ed by coastal terraces on
the southeast coast of Shikoku，Southwestem Japan．∫．Gεodα．8oc．ノαραη，ザo1．10，ρρ．116－122．
5．4．QuaternalIy tectonic divisioms of Japan
5．4．1．Method
Quatemary tectonic movement in Japan is regiona11y characteristic as shown in the maps of
vertical disp1acement and the distribution of Quatemaワfau1ts and fo1ds．Vertical disp1acement during
the who1e period of Quatemary attains to more than l，500meters in Central Japan and the Kanto
Plain，but it is Iess than750meters in other extensive areas of the country．1n Southwest Japan，it is
70一
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麗1。・一
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・中・十r。 一■ユ■
上≡…「irr
戸■十
里 〕 ムー一・一一 」■
！
■川…1卜・
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］ト1〔lj
一一一トー⊥．＿⊥．＿
ノ■ 一イ■㌃
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1D
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）
1 ■ ■＿二L■
〔4
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T 「■
1⊥
ぐ
1■1■l
l■．
■．」」＿＿」．
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Fig・5・13・Di・t・ib・ti… f・・1・…d・…gyby
…thq・・k・・i・hi・t・・i・p・・i・d（lo
meshes〕．
Fig．5－14， Distribution of densities of fau1ts
（1meshes）．
Fig．5－15． Distribution of densities of folds（lo
meshes）．Fig．5－16．Distribution of maximum uplift
amounts（1 meshes）I
■lO・O・
騒1川1〕o・w〕・
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〔〕1・・1ザOlll
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十十十｝
■州…I
口い□N□・1
∵プ皐・
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一．1．三軌1
llr
、粋」一一一一一■
（ 亜）．一．
≡r■
■■．L一、
，阯．＿、．．、。・
）
Fig．5－17． Distribution of maximum subsidence
amounts（l meshes）．
Fig．5－18． Distribution of gradients（1 meshes）． Fig．5－19．Distribution of coπected maximum
subsidenceamounts（1o meshes）．
Fig．5－20． Distribution of c01rrected gエadients
（1 meshes）．
contrastive1y much less in the Inner Zone than in the Outer Zone．The inner side ofNortheast Japan
is characterized by the dense distribution of Quatemary fo1ds，but the Kinki District by Quatemary
fau1ting・The Japanese Is1ands，therefore，can be c1assified into severa1Quatemary tectonic divisions，
according to the characteristics and intensities of Quatemary tectonic movement．
0n the other hand，some interesting relationships have been found between the late Quatemary
tectonic movement and the recent crustal deformation，especia11y seismic ones，In variOus regiOns of
Japan，it was inferred that the late Quatemary tectonic movement had o㏄ured in the modes and
areal dimensions simi1ar to recent crusta1deformation（Yoshikawa，1970），and that the rates of
tectonic movement had been uniform since the begiming of the Quatemary（Sugimura，1967）．
Tectonic movement，however，has not a1ways uniformly proceeded throughout the Quatemary period
in every region of Japan．For examp1e，in the inner side of Northeast Japan the mode of tectonic
movement is considered to have been uniform since the begiming of the Quatemary，but it changed
during the P1eistocene on the Pacific coast of Southwest Japan（Ota，1968）．Such a difference of the
sequence of Quatemary tectonic movement may be ascribed to that of tectonic history between the
above two regions．The historica1deve1opment of tectonic movement and its regional characteristics
during the Quatemary period shou1d be further e1ucidated in every region of Japan in future．For this
purpOse，it is necessary to prepare also the1ate Quatemary tectonic maps for the period of the order
of104to105years，together with the a1ready pub1ished maps for the whole period of Quatemary．
The Research Group for Quatemary Tectonic Map is now co11ecting data on late Quatemary tectonic
movement to compile such maps，but it is a mhter1aborious work to complete them．
From the above・mentioned it is considered that studies on Quatemary tectonic movement may
be usefu1for investigating the historica1backgrounds of recent seismic acitvities．A㏄ording1y，the
classification of Quatemary tectonic divisions wil1contribute to the arrangement of seismo1ogica1
observatories over the whole country for predicting the occurrence of future earthquakes，because it
wi11indicate summary regiona1characteristics of tectonic movement in the recent geologic time．
From this point of view，the Research Group attempted to divide the Japanese Islands into
Quatemary tectonic divisions and classify them as a conclusion of this report．This division and
c1assification was made only according to characteristics and intensities of Quatemary tectonic
movement，and character of seismic activities in recent and historic period in each division wil1be
mentioned1ater in the regiona1description of Quatemary tectonic divisions．
In the classification of Quatemary tectonic divisions，it is important to give due consideration
also to the regiona1differences in the g正adient and amount ofvertical disp1acement and in the mode
of tectonic movement，because zones of high gradients of vertica1disp1acement are usua11y
accompanied with fau1ting which is considered to have c1ose re1ation with seismic activities．The
gradients of vertica1displacement are obtained by measuring maximum differences of vertica1
dilplacement with㎞squarel of15’㎞1o壇tude and13％in1atitude（about25x25㎞）in
QuatemaW Tectonic Map Nos．1and2．They are c1assi丘ed into8grades and are sho㎜in a
distribution map（Fig．5－21）．Then，the Japanese Is1ands are tentative1y divided into10Quatemary
tectonic divisions，judging from the regiona1differences of amounts and gradients of vertica1
disp1acement during the whole period ofquatemary．Boundaries ofthe Quatemary tectonic divisions
generauy correspond to the significant tectonic 1ines or other discontinuities in geo1ogical and
geomo叩ho1ogica1structure（Fig．5－22）．
Another support for our division may be provided by Tab1e5－4．The activities of tectonic
movement are represented by average absolute amount and gradient of vertica1disp1acement during
the whole period of Quatemary in every division．These va1ues could be easi1y c1assified into three or
four classes as shown in Table5－4．It is very interesting that frequency distribution of absolute
amounts and gradients of vertica1disp1acement in every c1ass or division is characteristic，which may
be caused by the characters of Quatemary tectonic movement．This suggests that the above
Quatemary tectonic division is proper。
71
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27
The distribution of Quatemary faults and fo1ds is very important for revea1ing the modes of
Quatemary tectonic movement，and is considered to be c1ose1y re1ated to recent seismicity．To
represent densities of fau1ts and fo1ds，numbers of them with㎞squares of15’in longitude by13％1
in1atitude were counted in Quatemary Tectonic Map Nos．4and5，and then the squares where more
than five fau1ts or fo1ds are distributed were defined as squares dense with fau1ts or fo1ds and the
squares where four or three faults or fo1ds are distributed were defined as fairly dense squares．The
distribution of fau1ts or fo1ds in every division was judged from numbers of squares of these two
㎞dsasshowninTab1e54．lnotherwords，divisionswherefau1tsorfo1dsaredense1y砒stributedin㏄rtain1imited areas were judged to be higher in their density than other divisions where they are
even1y distibuted，when the tota1numbers of faults or folds were the same in each division．
The c1assi行cation of Quatemaワtectonic divisions was attempted for the purpose of
contributing to the prediction of earthquakes．In c1assifying the divisions，the工efore，Particu1ar
attention was paid to the density of fau1ts among the above three e1ements，because it was considered
to have co1se relation to seismicity．From this point ofview，the gradient ofveritca1displacement a1so
is a veW㎞portant e1ement，because not a11of Quatemary fau1ts cou1d be picked up in Quatemaワ
Tectonic Map No．4，and because zones of higher gradients in vertica1disp1acement are usuauy
accompanied with fau1ts．After the above considerations，the Quatemary tectonic divisions of the
Japanese Is1㎝ds were c1assified into five c1asses as shown in Tab1e54，and emphatica11y considering
gmdients of vertica1disp1acement and denstites of faults，divisions where both the va1ues are higher
than in others were expressed with the sufOx“十”amoung divisions belonging to血e same c1asses．
Activities ofQuatemaW tectonic movement we正e more intense in the a1phabetica1order．
5．4．2．Regio皿a1description
The study on Quatemary tectonic movement by the Research Group of Quatemary Tectonic
Map has not been extended on submaエine bottoms around the Japanese Is1ands，md therefore，it was
impossib1e to decide ocean－side boundaries of
the Ouatemary tectonic divisions according toc。、、、ct、、、。ft，ct。、ic。。、、。、、t㎝。㏄m 1！
bottoms．Seismic energy of recent earthquakes 2
was calculated as shown in Fig．5－12，but most
of recent earthquakes in and around the
Japanese Is1ands originated off the Pacinc
coast．From this reason，tota1amounts of 4
・…gy・・1・…dby・・…t…thq・・k・・…1d 4’ 3not be estimated in individua1tectonic divi－
sions． It is， therefore， difficu1t to discuss 6 5
on seismic energy of recent earthquakes in 8 7 8
each division，and it is very urgent to corfirm ，
th・・・・・…id・，・・p・・i・1lyP・・ifi…id・b…d－ 9 〃 、・・i…fth・Q・・t・m・・yt・・t・・i・di・i・i㎝・， ？．
where epicenters of most ofrecent earthquakes 』’一一 〇4 ・＾
were1ocated．Genera11y speaking，however，it is
…yi・t・…ti㎎t・工・c・g・i… t㎝d㎝・yth・t Fig．5・22Q・・t・m・・yt・・t・・icdi・i・i・…fJ・p・・。
the K…mto and Kinki－Nobi divisions have 1：Northem and Eastem Hokkaido，
re1eased more seismic ene㎎y，where gradients 2：Hidaka・Yubari，3：mtakami・Abu・
of vertical disp1acement are rather hi虫com－ kuma，4：The Imer Side of Northeast
pared with its absolute amounts・ Japan，5：Kanto，6：Centra1Mountains，
D：Northem and Eastem Hokk地do・1n 7：Kinki・Nobi，8：Chugoku－Setouchi，
this division，hms most1y lower than1，O00m 9：Kyushu，10：The Outer Zone of
extend and short rows of valcanoes are distri・ Southwest Japan．
73
buted’ε〃θo加1o〃，trending NE and extending east－northeastward to the Kurile Islands．The
amounts of vertica1displacement are mther sma11and its gmdients are1ow．Quatemary fo1ds and
fau1ts are recognized in the northem・and eastem・most parts of this division．Recent seismic activity
is1ow and no remarkable seismic crusta1deformation has been found in recent times．
B：Hidaka－Yじbari．This division is composed of two NNW・trending mountain ranges and a
depression which separates Hokkaido into the main and peninsu1ar parts．The maximum amounts of
up1ift during the Quatemary exceed1，000m and those of subsidence exceed500m．Quatemary
fo1ds are rahter dense1y distributed，trending N・S in the westem part of this division consisting of
Tertiary formations．Seismic activity is very high off the south coast of this division，but any
remarkab1e seismic crusta1deformation has not been recognized on the1and of the division．This
division is very similar in such characteristics of seismic cmstal deformation to the Kyushu Mountains
1ocated in the westemmost part of the Outer Zone of Southwest Japan．
E：Kitakami＿Abukuma．This division consists of two iso1ated mountains，distributedθ〃
θc加1o〃on the Pacific coast．Both of these mountains main1y composed of Pa1eozoic and Mesozoic
rocks and characterized by p1ateau・1ike features，because erosion surfaces extensive1y extend，and
they are separated by mmows basins from the mountain ranges in the Inner Side ofNortheast Japan，
The boundary of these two divisions conesponds to the zone of high gradients in the distribution of
Bouguer’s anoma1ies of gravity．The amounts of uplift are most1y1ess than500m and its gradients are
low．Recent seismicity is extreme1y active off the east coast of this division，where the deep Japan
Trench extends near1y para11el to the coast，whereas it is very imctive in this division．
C：The Inner Side ofNortheast Japan．This division is a Neogene fo1d zone and is chamcterized
by successive activities of folding in the Quatemary，by which fluvial terrace surfaces and even a1luvial
p1ains have been gent1y deformed．This division，inc1usive of the peninsu1ar part of Hokkaido，consists
of two para11e1mountain ranges，sma11basinsintervening血e ranges㎝d the1ow1ands on the coast of
the Japan Sea．Many volcanoes are distributed a1ong these mountain mnges．Veれical displacement is
genera11y not so1arger，and it si1arger in its sou曲em part．The max㎞um㎝ounts of up1ift is1，000
mandthoseofsubsidence500mintheNiigataP1ajn．Inthisdivisionrecentseismicityismtheractive，and dip－slip faulting as we11as active fo1ding has been recognized at times of recent
earthquakes．
A：Kanto．This division consists of the Kanto Plain and its surrounding mountains．The Kanto
P1ain is a tectonic basin having grown since the Miocene，and its centra1part has subsided by over
1，500msincethebegimingoftheQuatemary．Up1andsurfacesextendinginthep1ainhavebeengent1y undu1ating1y deformed since the late Quatemary．The frequency distribuiton of gradients of
vertica1disp1acement is bimoda1，beccuse the marginal parts of the Kanto tectonic basin have been
deformed with very high gradients，whereas the surrounding mountainous areas have been up1ifted
with rather low ones．Vo1canic areas extend in the surrounding mountains and the westem part of
this division was subject to fo1ds in the Neogene and since then has been up1ifted．This division
suffered extensive uplift and subsidence by recent earthquakes and is one ofthemostactive regions
in recent seismicity in Japan．Its southem part is very simi1ar in features of seismic crustra1
deformation to the Outer Zone of Southwest Japan，md therefore，is considered to be the eastem
extension of the latter from the viewpoint of the seismic division．
A＋：Centm1Mountains．This division occupies the highest part of the Japanese Islands and
three high mountain ranges，the so－ca11ed Japan A1ps，extendθ〃εc加1o〃，trending NNE，The highest
parts of the mountain ranges a1ittle exceed the height of3，000m above sea leve1and the amounts of
up1ift during the whole period of Quatemary are most1y more than1，000m．Gradients of vertical
disp1acement are genera11y very high，especial1yカong the margina1parts of the mountain ranges
which are bordered by huge fau1t・scarps or steep fiexure・scarps．It is very curious and noticeab1e that
this high1y active division in Quatemary tectonic movement is very inactive in recent seismicity and
has not suffered remarkab1e seismic crustal deformation in recent times．
74
C＋：Kinki－Nobi．This division is characterized by sma11tectonic ranges and basins．Erosion
surfaces formed in the1ate Tertiary have been dislocated at various heights and part1y preserved on
tops of mountain ranges，and basin floors have subsided by more than500m in the Osaka and Nobi
P1ains．In genra1，gradients of vertica1disp1acement are not so high，but they are1oca1ly very high
釦ong Quatemary faults which are densely distributed，bordering the mountain ranges in this division．
Some of the Quatemary fau1ts have been dis1ocated horizonta11y as we11as vertical1y．This division is
very active in recent seismicity and it is very interesting that there．are some strike－slip seismic fau1ts at
times of recent earthquakes in the division，which are very simi1ar in mode to the Quatemary fau1ts．
E：Chugoku－Setouchi．Plateau・like mountains300to500m high extend，and rahter isolated
sma11mountain b1ocks a little higher than1，000m form a back－bone range trending ENE．The
southem margin of the mountains gent1y descends down to the Setouchi inland sea depression，the
southem margin of which is bordered by the Median Tectonic Line．In most parts of this division，
amounts of uplift are less than500m and its町adients are lowest in Japan．Several Quatemary fau1ts
but no fold have been found in this division．Recently an earthquake occurred in a1oca1area，but
recent seismicity is rahter inactive and seismic cmsta1deformation a1so was very loca1．
D：Kyushu．This division consists of the remain of Kyushu Is1and exc1uding the Kyushu
Mountains which belong to the Outer Zone ofSouthwest Japan．In the northem ha1fofthis division，
sma1l b1ock mountains are distributed，intervened by1ow1ands，and low hi11y lands in its westem and
southem parts are covered with1ava f1ows．The southem ha1f of this division，including Aso vo1cano，
is・ha・act・・i・・dbythe・xiste・ce・f鹿・・tic・・1d・・・…dth…t…i・edist・ibuti・nof・p1・・ds
composed of pyroc1astic sediments．Amounts of up1ift are1ess than700m and its gradients are low．
Recent seismicity is very inactive and no remarkable seismic crusta1deformation has been recognized．
B1The Outer Zone ofSouthwest Japan．This division is bordered by the Median Tectonic Line
along its northem margin，which has been dis1ocated horizonta11y as we1l as vertica11y in the late
Quatemary．This division is separated into three main parts，that is，the Kii，Shikoku and Kyushu
Mountains，by narrows straits．Amounts of up1ift in these mountains duhng the Quatemary exceed
1，000m，and it has been considered that this division have been undu1atingly defoTmed with
wavelengths of about150to200km since the begiming of the Quatemary．The eastemmost part of
this division is piedmont areas of the Centra1Mountains．Up1and surfaces extending in this area have
been gent1y undulatingly deformed with axes trending NE in the1ate Quatemary．Recent seismicity is
very active off the Pacific coast of the division，and the division suffered characteristic seismic crusω
defo㎜ation by recent earthquakes，which was considered to have v町interesting re1ations with
Quatemary tectonic movement．In the Kyshu Mountains，however，any remar㎏b1e seismjc crusta1
movement has not been found，in spite of active seismicity off the coast east of the mountains．
In conc1usion，there are a few interesting re1ations between recent seismic activities and
Quatemary tectonic movement in each tectonic division．These relations，however，shou1d be further
examined，considering the historica1sequences of tectonic movement in the Quatema町，which are
to be so1ved for every Quatemary tectonic division in future．At the same time，it is very important to
study the tectonic movement on submarine bottoms around the Japanese Is1ands，where the
epicenters ofmost of recent earthquakes were1ocated．
5．4．3．Refe1－ences
Ota，Y．（1968）Deformed shore1ines and1ate Quatemary crusta1movements in Japan・Mem・Geo1・
Soc．Japan，No．2，PP．15－24．
Sugimura，A．（1967）Uniform rates and duration period of Quatemary earth movements in Japan・
J．Geosci．0saka City Univ，Vo1．10，Art，1－4，pp．25－35．
Yoshikawa，T．（1970）0n the re1ations between Quatemary tectonic movement and seismic crusta1
deformation in Japan．Bu11．Dept，Geogr．Univ．Tokyo，No．2，pp．1＿24。
75
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一76
6．Postscript
The work for compi1ation and pub1ication of this vo1ume was commenced in1963by the
fol1owing7persons：K．Hatori，S．Kaizuka，Y・Naruse，Y・0ta，A・Sugimura，H・Takahashi and T・
Yoshikawa．
Thereafter at present as of Janua取1973，the fo11owing5persons are added to the members
for the work：R．Ishii，C．Komori，F．Shimizu，M．Takahashi，and N．Yonekura．
Partia1charge of the work for prepamtion of Tectonic Map was assigned the person（s）named
be1ow，as fo11ows：
1．Vertic釦disp1acement estimated by geomorpho1ogica1method：Kaizuka，Ota，Yoshikawa，
Yonekura．
2．Vertical displacement estimated by geo1ogical method：Hatori，Naruse，Ishii，Komori．
3．Vertical disp1acement compi1ed from the Maps Nos．1and2：All members．
4．Distribution offaults：Sugimura，H・Takahashi．
5．Distribution of fo1ds：Kaizuka．
6．The Gipfe1f1ur Map prepared by Prof．T．0kayama was offered us by the courtesy of the author
and was added as a part ofthe Tectonic Map．
Partial charge for the mmuscripts ofexp1anatory text is as fo11ow：
1． Yoshikawa．
2．1．1． Yoshikawa．
2，1．2． 0ta，Yonekura，Yoshikawa．
2．2．1． Yoshikawa．
2．2．2， Hatori，Naruse．
2．3． Yoshikawa．
2．4． Yoshikawa．
3．1．1． Yoshikawa．
3．1．2． Sugimura，H．Takahashi．
3．2．1． Yoshikawa．
3．2．2．＿3．2．5 Kaizuka．
3．3． Yoshikawa．
4． Yoshikawa．
5．1． Sugimum．
5．2． Kaizuka．
5．3． H．Takahashi，M．Takahashi．
5．4． Yoshkawa，
6． Sugimura，H．Takahashi．
7．1． Hatori，Shimizu．
7．2． Naruse．
7．3． Sugimura，H．Takahashi，Shimizu．
7．4． Kaizuka．
7．5． Al1members．
一77
7．
7．1
1．
2．
3．
4．
5．
6．
7．
ApPemdices
Listo川epres㎝川eightsofgeo1ogicfo㎜ati㎝s．
Number（Quadrang1e number and1oca1ity number）。
Nume制㎝themap，whichindicatestheheightofgeologicfomation（unit：10m）
si即on numeral horizons of formations coefficient for giving the amount
of up1ift during the Quatema収
sign1ess Up．P1io．，Low Pleist． X1
［ l Low．P1io．o㏄asiona11y Up．Mio． X1／2
（ ） Mid．Pleist． X3
（（（ ））） Up．P1eist． ×10
（（ ）） Doubtfu1case
Location（number of l：200，000topographic map and1：50，000topographic map）．
Height ofthe geo1ogic formation（in m）．
Evidences（Formations and their．age）。
References（Descriptions are shown in the fo11owing order：author’s name，year of pub1ication．
Refferred geo1ogical maps are indicated with the kinds ofmaps as fo11ows：
V： 1：50，000；VlI：1：75，000；XX：1：200，000；L：1：500，000）．
Note．
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？： direction of throw unknown．
E nd＝ east throw，quantity unknown．
S100： south throw，100m．
E120＊．： （＊：horizonta1slip，estimated at0）．
EndR： east throw；throwun㎞own；right horizontal slip－
N〈0．75R〈1．5： north thエow0．75km and less；right s1ip，1．5km and1ess－
WndTh：westthrow；th∫owunknown；reversefault．
S＜500R＜5000：souththrow；throw，lessthan500m；正ights1ip，lessthan500m．
NW・ddip：50NW：…thw・・tth・・w；th・・w・・㎞・w・；dip50“W・
L nd： left s1ip；quantity unknown．
Evidences．
References（Descriptions are shown in the fouowing order：author’s mme，year of pub1ication・
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V：1：50，000，V1I：1：75，000，XX：1：200，000，L：1：500，000）．
p．c．：abbreviation of“persona1Communication”．
Reference number of abstract．
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7．4．
1．
2．
3．
4．
5．
6．
7，
8．
List of fold．
Number（Quadrangle number and fold mmber）．
Name of fo1d or p1ace．
Location（number of1：200，000topographic map and1：50，000topographic map）一
Name of folded stratum or geomorphic surface and the geo1ogic age and environment of its
formation．
Tc： Tachikawa age（late1ast glacial）．
M： Musashino age（early last創acia1）．
S： Shimosueyoshi age（1ast interg1acial）．
T： Tama age（penultimate interglacia1）。
Ld： Lower P1eistocene．
D： P1eistocene．
Pd： Plio－Pleistocene．
UP： UpPer Pliocene．
P： Pliocene．
m： marine．
f： f1uvia1．
Strike and1ength（in km）of axis．
Wave1ength（in km）；“F”：a㏄ompanied with fault．
Ang1e of s1ope on a1ib offo1d（in tangent and degree）；“F”＝accompanied with fau1t．
Rate of deformation or ve1ocity gradient（tan．1『5／103years）；“F”：accompanied with fault．
Ca1cu1ation is based on the following estimation of abso1ute age．
Geo1ogic age
Tc
MST
Abso1ute age
2．5・104y・a・s
5 x104
9 x104
25 x104
Geo1ogic age
Ld
Pd
UP
P
Abso1ute age
1・106y…s2x1064x1067x106
9． References（Descriptions are shown in the fo11owing order：author’s name，year of publication．
Referred geo1ogica1maps are indicated with the kinds of maps as fo11ows：
V：1：50，000，VII：1：75，000，XX’1：200，000，L：1：500，000）．
10． Reference mmber of abstract．
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昭和48年3月27日 印刷昭和48年3月31日 発行
欝薯国立防災科学技術センター 東京都中央区銀座6丁目15番1号 電話（03）541－4721郵便番号104
印刷所㈱昭和工業写真印刷所 東京都港区三田5丁目14番3号