conglomerates the northern fossa magna …

The Association for the Geological Collaboration in Japan (AGCJ)

NII-Electronic Library Service

The Association for theGeological Collaboration in Japan{AGCJ)

EAIITH SCIENCE ; JOURNAL OF THE ASSOCtATION

COLLABORATION IN JAPANFOR GEOLOGICAL

Vol. 24, No. 4. pp. 115N12S July 1970

NEOGENE CONGLOMERATES AND

NORTHERN FOSSA MAGNA INCENOZOgC

GEOHISTORY OF THE

CENTRAL JAPAN (Part II)"

by

TeruoHIRABAYASHI**

V Result of the Study

In this chapter the resuks of the study are

described according to geological ages, The

number and the name of the investigated localities

are given in Table 2. The geographic locationsand the stratigraphic position of the rcspective

localities are shown in Fig. 5. The materials

treated in the study are summarized in Table 6,

Fig, ].O (A-G) are pie diagrams showing the average

diameters of pebbles and the abundance ratios of

the component rock type at the localities groupedby formation.

Description of the datailed results of the investi-.cratiens ef each Iocality is omitted in this report.

Fig, 11 is bar charts showing the abundance ratios

of the component rock kinds.

VI Considerations

In this chapter the geo!ogical history of the

Northern Fossa Magna will be considered mainly

on the basis of the results ef investigations of theNeogene conglomerates.

A. Pageag'ene

!nside the Northern Fossa Magna, distribution

ef the Paleogene system is unknown, and theNeogene system lies directly on the Pre-Tertiary

basement. But few students are of the opillion

that the Paleogene system is distributed in Saku

Mountains, And the Ishizaka liparite seen in the

Otari upheaved zene <Hu{ABAyAsHi, 1969) has beendated 58 million years old, but no Paleogene sedi-

mentary rocks are diistributed there, However,these distributions are seen outside the NorthernFossa Magna.

B. Early Miocene

The litholegy of this peried is represented by

green tuff. IIoweve]', the depcsiticm of green tuff

*

**

Matsumoto Branch

was preccded by ordinary sedimentary recks as

observed in Mt. Moriya, in the I{achibuse Moun-tains, in the north of Ueda City and in the SakuMountains (Fig. 2),

The center of deposition of these sedimentary

recks was lccated west of the Median belt of

upheaval, and conglomerates are well develepedthere, In the east, on the othcr hand,the volcanicactivities that accumulatcd green tuff took place, The detrital inaterials during those times musthave been supplied from the Akaishi Mountains,the Ryoke belt along the Tcnryu River, and fromthe area in the south extending from the southernKiso district to Gifu Prefecture (Fig, 12), Thefirst two areas are close to the place of deposition,but the latter is quite distant, 100km from the pre-sent exposures. This would leadi to the followingassumption : a single great rlver was fiowing at thattime from the Kiso district, whereas minor rivers

were corning from the Akaishi Mountains and theTenryu River draina.ue area to join in the basin. In the Mt. Moriya arca at the northern end ofthe Ina Mountains, the Neogene system rests

un-

conformably on the Paleozoi'c system, The pebblesbecome larger in size, and Iewer in roundness

toward the upper horizons, suggesting the increaseof the amount of upheaval ef the hinterland, Atthe Hachibuse Mountains the conglornerate in thelower part contains pebbles of the Yol<okawagawametamorphic rocks that are exposed on the imme-diate east, Toward the upper horizons, durablechert increa$es in number, while slate decreases.

The reck types which indicate that the supply

source of pebbles was in the south at that time,are the Nohi t},pe quartz-porphyry (so-called Nohi-liparite), the sandstone of the Todai formation 'the Ryoke type granjte and the Sanbagawa typemeta;norphic rocks. It seems that almost

no

pebl)Ies were supplied from the IIida Mountains

The Dactor T]iesis presented to Kyoto University.Teachers' Consultant of the Nagano Prefecture Education Cci'iter and Instructor of Shinshu tmiversity



The Association for theGeologicalCollaboration in Japan {AGCJ)

116A)

Moriya andUchimuraformations

c)Aokiiormation

B)]3esshoformation

D) Ogawa formation

/'/

caiii

I1/

l



TheAssociationfortheGeologicalCollaboration in Japan {AGCJ)

117

E)Shi igaramlforrnation

9

F) Sarurnaruformation

G)Toyonoformation

1/

chertgrarvackes)ateg

harnfe16

sandsteneeenglemeTate

mudstene-1

greentUffil

dacite(Omine

anaes ±tety?e)

liparite(a]terated

N

Fig.10.Pieand

legend

aacite)

CX: point

basaLtporphyrite

dior ±te(TerLiars

guartz-porphyry

granitevelnquartz

Eerpentinite

crystalline

gnelSSotherrecks

granite)･

schist

O-.-.t.ny-.h.O 20im

ot :oealM7)

diagrams showing rock cornposition

pebble size for each formation.

(The numerals in thethe.Iocality number inmeter of one fourth of

of onehundredpebb!es

figures comcide with

Table 2, and the dia-the average diameter

at each locality).



TheAssociationfortheGeologicalCollaboration inJapan{AGCJ)

1

!18

Meriyaformation

Uch ±rnuraformatien

Besshoformat ±en

Aeltiformat ±on

t±on

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16a81921222J2425

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Legend

4o

yvV ss+t-"tl

(The Fig. 11,

numerals in

riac],te(Uchlmura F.

++++++i"ltixm-f+zauu"uuulslt"e"lluuu"

5o 6o 7o o ee1oo

EEff.pg!pgtl;ite

glLartz-d ±orite(Tertiaranite)

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se!p!nXtnl"te(ultrabastcrock

!i'ISV.q]1±neshi.st

{pelssifherrockE t-tt-tt--....ttt'

Rock composition of the conglemerates in each locality.

the left side of figures coincide with locality nurnber inTable 2)



The Association for the GeologicalCollaboration inJapan {AGCJ)

119

A) Meri raandVchimuraAges

E

B) Besshe Age

r

L..

/ it/

a

C) AekiAge D) Ogawa Age

N; Nagano Ceo; Orna¢ hi c,M;

NatsumoteH; Haknba V.

!

C. U; Ueda C.---'Center

ofS;

Suwa C. Sa;Median Belt of

1/

a

saku c.Upheaval



The Association for theGeologicalCollaboration mJapan {AGCJ)

120

E) Shigarami Age F) Sarumaru Age

G)

/

Toyeno Age

Sa

/

-m

N

,,p

s

va

fi p gg # o x

e･s

N

+/

Fig. 12,Supply source inferred for each age.

(The dotted areas show the present exposures of each formation.the pebble direction and strength of transportation).

O 20km'

The arrows show



TheAssociationfor the Geological Collaboration in Japan

in the west. This is perhaps for the reason that

the amount of erosion was smaller on the east

side of the Hida Mountains than in the Akaishi

Mountains or the Kiso Meuntains, or that the iorce

of the coastal current from thc seuth was strong.

In those times, great ciuantities of pebbles were'

supplied into the Southern Fossa Magna on the

east side of the Akaishi Mountains.

In the Toyarna sedimentary ba$ln, northwest of

the Hida Mountains, the Hokuriku group, ranging

in age from Miocene to Pliocene, was deposited

with the total thickness exceeding 5,OOO m (SAKA-MoTo et al., 1959). The hitherto prevalent vicwthat the Hida Mountains is tilted westward may

have been deduced frorn the mode of erosien.

The Early Miocene "green

tuff," which was de-

posited in the eastern area, is locally intercalat'edwith ordinary sedimentary rocks such as sand-

stone and mudstone. This suggests that thick

beds of green tuff are a result of well-balanced

subsidence and sedimentation. Thus, the ejecta of

submarine volcanoes were successively depositedin the eastern area where the amount of sub-

sidence was great, and supply of pebbles frorn the

surrounding older rocks was very little, In the

western area, on the contrary, transgression

occurred somewhat later than in the east, and

flysch-type deposits were accumulated, In both

areas, the depositional plane was in a roughly

identical cendition during the same stage, and the

strata of the eastern area interfingered with those

of the western area. The western area is inierredto have undergone warp-like subsidence. And

pebbles were supplied from the Akaishi Mountains

and the Kiso district in the south. However,

evidences verifing the view that the eastern area

made an anticlinal upheaval and abundantly sup-

plied deposits into the western area, are scarce

except fer the fact that sorne amounts of tuffa-

ceous materials were transported. The conglomerate developed in the Uchimura

formation north of Matsumoto City is distributed

in an E-W direction. Any variations of rock

types or pebble sizes due to the place of depositionare not recognized, which may suggest that the

main stream coming from the Kiso district had

branched out into distributaries here befere itfiowed into the sea of those days.

During the Uchimura stage, intrusion of pha-colith (esoplith)-like porphyrite took place, injecting

or disturbing the strata. The porphyrite is sup-

posed to be contemporaneous with the quartz-

diorite belonging to the folding period of the Bessho

phase (KoBAyAsm, 1957). Dating of the quartz-diorite shewed 8.5 milliQn years, which is quite

{AGCJ)

121

young (Fossa Magna, 1968).

Toward the encl of the Uchimura stage, basicvolcanic activities, represented by basalt, becameviolent in the eastern area. The basalt is partiallyspilite or has a pillow strueture, and is locallyintercalated with argillaceous bcds which are called

Kokuzo member, being 600m at the thickest.

Above this lies the 1;ujisan member, as thick as

1,500m, charaterized by acidic velcanlc rocks.

Though decreasing in thickness the Fujisan

member extends far into the western area. Itslithology is composed of pyroclostics of glassyandesite and dacite, with intercalations of sand-

stene, mudstene and tuff breccia. Both Kokuzo

and Fujisan rnembers have been altered to green

rocks which, in the form of pebbles, are to betransported out during the post-Uchimura stage,

C. Mialdge vaocene

The Bessho stage is known as a period of sudden

increase in the amount of subsidence and expan-

sion of the marine region, Abnormal sedimenta-

tion is eften observed in the rock facies, but on

the whole the deposits were laid dowz in a calm

envlronment. '

From the end of the Bessho stage to the Aekistage, the ameunt of tran$ported pebbles becornes

larger. The area where the Uchimura formationwasdepositedwasupheavedanderosienbegan, The

felding of the Bessho phase was followed by the

intrusion of quartz-diorite and porphyrite; the

existence of the median belt of upheaval becameconspicuous, by which the Northern Fossa Magnawas split intQ two sedimentary basins, east and

west, as verified by the sedimentary facies revealeclthrough the study of pebbles. However, putting

aside the median belt of upheaval, the writer drewthe Matsumeto-Nagano line (HiRABAyAsHi, 1969) tocompare the eastern and western areas, by taking

into account the structural differences between

these two areas.

Successively irom Early Miocene, thick ordinarysedimentary rocks were deposited in the western

area. Rock composition of pebbles is relatively

sirnple. But, in Middle Miocene, chert begins to

increase while the Nohi type quartz-porphyry de-

creases, both becoming smaller in pebble size. Asthe cause of this phenomenon, an increase in thedistance of transportation and a topographical

change in the hinterland may be considered. In

those days, pebbles were supplied mostly from the

south, not from the Hida Mountains in the west

in spite of the short distance. The major river

systems may have been roughly the same as those

of the Early Miocene period, Judging from the

high degree of roundness and the small diameter,



TheAssociationfor the Geological Collaboration in Japan{AGCJ)

122

some of the pebbles may be derived pebbles frornthe Early Miocene deposits,

The Middla Mioccne deposits are centinuos over

t.he eastcrn and western basins, though they are

thinner in the median belt of upheax,al, Theamom]t of upheaval of this belt mav･ ]tavc 1)eciismaller in the Ueda City area.

In the east of the median t)elt of upheax,al,

pebbles of volcanic rocks from the area of greentuff of the Uchimura formation begin to appear inthe strata o/E the latest p6riecl of the Bessho stage,and they keep on increasing duTing the carly

period of the Aoki stage, But, they never Teached

the western ba$in beyond the median belt of up-

heaval. Accordingly. it is considered that the

water systern at that time was different betweenthe eastern sedimentary basin and the western

one, and only the fille-grained deposits were dis-tributed in these two basins beyond the median

belt of upheaval, On the other hand, the Nohitype quartz-porphyry, which is abundant in the

western basin, is found to have been transported,

though in a srnall amount, down to the vicinity

oi Ueda City. This fact may be explained byassuming the existence of a coastal current flow-ing from west to east, as will be supportedi by thecrossbedding in the sandy parts indicating an

eastward flow (near Mameishi Pass). Tbis as-

sumption is based on the impossibility of trans-

portation of the Nohi type quartz-porphyry fromthe Kanto district side.

In the eastern sedimentary basin, with an in-crease in the abundance ratio of the Tertiarypebbles of the Uchimura stage, the pel]bles of

Paleozoic rocks decrease, However, the Paleozeic

pebbles are generally larger in sizc and lower inrounclness than those found in the western basin.So, these pebbles were supplied probabl)' from theSal{u Mountains. In the distribution area of theUchimura forrnation on the south side of the

sedimentary basin, there are no beds that could sup-

ply derived the pebbles of Paleozoic rocks. There-'fore,

the water svstcm frorn the south must have -been developed in the eastern basin, too. Thiscan be deduced frem the presence of pebbles of

suppesedly Mog. iyama granite, as well as the peb-bles of Paleozic rocks.

In this peried the quartz-diorite body intruding

the Uchimura formation does not occur as pebbles

yet. Along the Saigawa folded area, pebbles ef

green tuff and the Sanbagawa type metamorphic

rocks are abundant. The reason of their presenceremains unexplained, although it is possible thatthe rocks in the lower horizons were squeezed up

during the disturbance.

In the area around the Otari upheaved zone,

date are scarce and the stratigraphic division hasnot. been establis]]ed, so the wrjter refrains frotncliscussing the g,eological history ef this period.

D. .ILale A･fiocane

ln this 1)eriud the sedinienl.ars･' Ijasins on boLhsidc,,s of the median belt of upheaval were com-

pletely･ separate from each other, and were filledwith different deposits, In tbe western sedimentarv basin the marinc

deposits were accumulated successively over a

wide area. Due to the folding after the deposition,the distribution ef the depDsits as seen today seems

to indicate a stTong ernbayment at that time. But,

as the rock types of pebbles are markedly variable

with the place of deposition, it is considered that

the coastline of those times was fairly situated,

and pebbles were transported and deposited by

streams of various river sv･stems,

It is characteristic of this peried pebbles began

to be supplied also from the Hida Mountains inthe west, while the supply from the south de-creased and perhaps only some derived pebbleswere transported into the basin,

The average diarneter of pcbbles of the Ogawastage is 27.9mm, smallcr than 32,6mm of the

Aoki stage. This tendency viewed from the

largest pebbles is illustrated in Fig. 13. Pebbles inthe respective formations of the Northern FossaMagna are apt to beceme larger as tlie age be-comes younger. The Ogawa stage Iacks this

general tendency, This is probably ascribed to

the topcsrraphic conditions of the hinterland, that

is, the supply from the south lessened due to theobstruction by the median belt of upheaval and

yet the erosion and transportation irom the HidaMountains were not much adyanceel to replenish

the supply.

The fact that the pebble size decreases eastward,iiamely, toward an inner part of the Fossa Magna,

and the abundance ratio of durable rock types

increases would prove that the main source of

supply was on the IIida Mountains side.

It is interesting that, as the age becemes yeunger,tho rock types of pebbles in the Fossa Magna

change from Paleozoic rocks to shallow-seated

igneous rocks and then to granite, keeping pace

with the progress oE erosion into the deeper partsof the Hida Mountains. Judging frem the sites of rocks now exposed in

the Hida Mountains, the place of deposition is evi-

dently in the north-northeast. One of the reasons

for its location may be the north-lateral pressureexerted irom the east side of the Otari-Shiojiri line

a.aainst the west $ide, causing the leitward hori-



The Association for theGeologicalCollaboration inJapan {AGCJ)

123 ,

Srt- - t

-t

1'

, ,l i･ S-ilkresi-- "u･

i

"---T

-N-l- ------

-

-

-

l -7

----- .!.r

.lj.2/gl;.,

llev L

...i

-VB;L.--'fi,;'l

z..,

.

''

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/ I

i:

g

,,:i`tt

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.--

it- - -d-;.--

Ft -# tj tt

---

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{i

:'; .･.,･le

. ff. .i

･xz.

iil ' = "

--t

.+

z

malgOFF;7}.){l;f!L!IY.,"-wu "-

v"

･- Lr'

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t

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oapt--=lgm-mmego km

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---

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E'il'o'gr=-tJILN !

llifilllew

tw.i

± [-.-Ld.=.).-utt

iiiiilV i,[v

t

1fift1

Iilll11111

pi,,Vls:iSt

1riil-!i s L

x

NN.

x '

Les1

Q,,mi

tlz}t;;'

fr7ifijilfiYls:i-

..

,M)s

Las

g ogawa fortnatien Legend

am Sarumaru forrnation i"i:i[t Aoki formation IMIilli

:. :. ;.::. shigaraul

forrnation

EEII:EEI Bessho

forrnat ±on

Fig, 13, Distribution of maximum pebbles of Paleozoic rocl<s in each formation

(The diameter of each circle cerresponcls to one twentieth of the maximu,m size

pebble diameter in each locality),of




124

zontal displacement of strata, as mentioned befere,Nevertheless, the state of the later deposits and

the crossbedding seem to support the assumption

that the course of transportation was somewhat

deviated northeastward and the strong' coastal

current was flgwing [rom south te north.

From the end of the Ogawa stagc to the Shi-

garami stage. intermixture of andcsitic pebbles

becomes･ conspicuous, When inferred from the

rock types and pebble sizes, these andesitic pebblesmust have been derived from the volcanic activity

that toQk place in the Fossa Magna at the time

of deposition,

Deposits of the Ogawa stage in the eastern

sedimentary basin are exposed only at Komaki-

yama of Ueda City. The deposits seem to havebeen supplied from the surrounding areas, such

as the area in the north of Ueda City, the Uchi-

mura area and the Saktt Mountains area. Rock

types are various. Andesitic pebbles are abundant,

increasing all the more in the Shigarami stage.

Since the end of the Ogawa stage of Late

Miocenc, andesitic volcanic activities took place in

the Northern Fossa Magna ; the activities becamemore violent in the Pliocene, and have continued

to the Recent. This is verified also by the cha-

racter of pebbles,

E, l7iocene

In the Pliocene period, transporting force grewstronger rapidly. The average diameter of pebblesof the Shigarami stage is 40,4mm, and in the

Sarumaru stage it reaches 51,3 mm. This tendencybecomes remarkable as the age becomes younger,

It may be ascribed to the increase in the abund-

ance Tatio of the 'l]ertiary

pebbles transported

from nearby sources, but the pebbles of Paleozoic

rocks aTe also found to become larger in youngerdeposits, as shown by their maximum diarneterwhich averages 63.7 mm in the Ogawa stage but,increases to le7.2mm in the Shigarami stage and

97.1 mm in the Sarumaru stage,

In the Sarumaru stage ef Late Pliocene, the

amount of upheaval of the Hida Mountains against

the Fossa Magna increased rapid!y, so that a pied-mont subsiding area was formed on the east side,

and molasse-type sand and gavel were depositedthere. During the sedimentation, the volcanic

activity represented by the Omine type dacite oc-

curred in the N-S direction, In the western sedimentary basin, the deposits

of the late Shigarami stage were transported north-

northeastward from the Hida Mountains, Thistendency is similar to the case of the Ogawa stage,

The deposits are distributed along the major syn-

clinal axes. Pebbles oi the Takase type granite

and the Nishina type quartz-porphyry are distri-buted in the Otari Mountains 30krn north-northeast

of the present exposures of these rocks, The close

resemblance of the conglo]nerate in the Nakatsuchlsyncline te the conglomerate in the Hikage syn-

cline may indicate that both conglomerates were

once in the same sedimentary environment, The

main movement of the Otari-Shiojiri line is a later

event.

In the Sarumaru stage, deltaic deposits were Iaid

down on the east side of the Hida Mountains.

The rock types of pebbles were markedly variable

with the rivers coming from the Hida Mountains

and fiowing eastward to enter the sea. The depositshave their source in the recks now exposed in the

IIida Mountains on the immediate west, Ne rocks

from the inner parts of the I'Iida Mountains are

found in the deposits, probably because the HidaMountains at that time was tilted to the west and

the rivers on the east side were small and short.

Almost on rocks from the Mt, Hakuba and its

vicinity were transported to the east, and the

Happo type serpentinite and the Hakuba type

metamorphic rocks are rare among the pebbles,This rnay be ascribed to the fact that the north-

eastern part of the Hida Mountains was not much

eroded, or that the east-fiowing rlver system was

not developed there. !t is true that these roc!{s

are undurable, but their occurrence as pebbles istoo small even among the recent river gravels

(Fig. 12).

The Pliocene depesits along the Susobana Riverinside Northern Fossa Magna are rnixed with

boulders of the Omine type dacite. These boulders

must have been transperted out oi the lava fiows

in the Omine formation (KoBAyAsm and HiRA-BAyi･xsHi, 1952) on the west side of the Otari-Shio-

jiri line at the time of the line's east-thTowing

movement aiter the sedimentation. Accordingly,

the horizon of the Sarumaru formation along the

Susobana River is higher than that in the Ominearea. The Pliocene series distributed in the drain-age area of the Susobana River consists chiefly of,

andesite of the Palaeo-Iizuna Volcano, but alse

contains exotie pebbles such as the Takase type

granite transported from the west-southwest, The

amount Df such pebbles, however, is very small in

comparison with their abundance in the recent

river gravels ef the River Sai-gawa in the neigh-

berhood,

As the time lapsed inte the Toyono stage, the

western sedimentary basin entered a fresh-waterenvironment for the mest part, and after the

tolding movement in the latest period oi the stage,

the block rnovement prevailed, causing the struc-



The Associationfor the Geological Collaboration in Japan{AGCJ)

125

tural upheaval of the IIida Mountains, the west-

throwing movement of the Otari-Shiojiri line, and

forming a basin structure between this Iine and

the Otari-Hakuba line (IIiRABAyAsHi, 1968). Since the Sarumaru stage, a fresh-water environ-

ment rapidly prevailed also in the eastern basin.Then the Kornore group was deposited, and a

little later the Enrei formation was deposited widely

extending as far as the Matsumote City area. These

deposits are of terrestrial origin. consistin.a largelyo/f pyroclastic rnaterials,

VII Conclusions

The iollowing geohistorical developments in theNorthern Fossa Magna were revealed through the

study of conglomerates.

A. Ileriod of suXiply from the south

During the Early te Middle Miocene period, the

supply source of pebbles was in the south, namely,

the Akaishi Mountains and the Kiso district, as

verified by the presence of pebbles of the Nohitype quartz-porphyry, the Sanbagawa type meta-

morphic rocks and the Ryoke type granite. I{owever,the deposits contaning the pebbles mentioned above,

are not founcl in the eastern sedimentary basin.

Green tuff of submarine volcanic origin was ac-

cumulated in the eastern basin, but no conglomer-

ate was developed there, The western area since

Early Miocene Was in an environment where

ordinary sedimentary recks abounding in pebblescould be deposited, Nevertheless, no positiveevidence is available to show that pebbles were

supplied from the Hida Mountains in the west or

from the Kanto Mountains in the east, The strata

ef the Bessho and Aoki stages, the period when

the median belt oi upheaval began to form, are

distributed continuously over the eastern and

western sedimentary basins, and the characteristic

Nohi type quartz-porphyry observed in the western

sedimentary basin is seen to have moved into theeastern sedimentary basin,

B. Pleriod of suPPly from the Uthimura fbrmation The green tuff, dacite and andesite of the Uchi-mura formation began to supp!y pebbles alreadyat the end of the Bessho stage of Middle Miocene,These pebbles were supp!ied mostly into the eastern

sedimentary basin, and were not transported into

the western sedlrnentary basin. Therefore, so faras assumed from the pebbles, the sedimentary

environment during the Middle Miocene was

strongly infiuenced by the eastward fiow of a

coastal current or a river system.

The quartz-dioritic intruding the Uchimura for-mation did not supply pebbles yet in this period,

There is a report (KoBAyAsm, 1957) on the

presence of the quartz-diorite among the pebbles

of thc Aoki stage, but it was not confirmed lnthe investigatien by the present writer. Trans-

I}ortation ei the quartz-diorite pebbles becoinesrnost conspicuous in the Pleistocene period.

C. I]taried of suiiply from variozas sources

At abeut the middle of the Ogawa stage of Late

Miocene, the rnedian belt of upheaval was developedremarkably, causing the eastern and the western

b4sins to undergo different sedimentations,

In this period the supply of pebbles from the

south into the western sedimentary basin clecreased,whlle the supply from the Hida Mountains on the

west began. In ether words, this was a tlansitional

period, As a eonsequence, the average diameterof pebbles became smaller than that of the Aoki

stage. Taking place of the Ryoke type granite,the granitc pebbles irom the Hida Mountains side

began to be intermingled, and the pebble size tends

to decrease eastward, going away frorn the Hida

MoUntains, Andesite pebbles are not found, andthe rock composition is rather simplc.

In the eastern basin the distribution of con-

glomerate is limited to a small area of Komaki-

yama. The component rock types are quite vari-

able, comprising the quartz-diorite in addition to

the volcanic rocks of the Uchimura formation fromthe Uchiyama area and from the north of Ueda

City, Pebbles of granite and Paleozoic rocks,

probably transported from the Kanto Mountains,are also found. Since this peried, the sedimentary

environment becomes entirely different betweenthe eastern and the western basins separated by

the median belt of upheaval.

D, Peptiod of sevpt)ly from the Eida Mbuntains

In the area along the Hida Mountains, namely

the western marginal zone oi the Fossa Magna,

the Miocene strata are not distributed, The older

rocks of the Hida Meuntains are directly overlain

by the strata of the Pliocene Sarumaru stage with

an unconformable relation (HIRABAyAs}ii, 1953), Inthe area east of the Otari-Shiojiri line, strata older

than the Shigararni stage are also distributed.Accordingly, the pebbles supplied from the HidaMountains into the Northern Fossa Magna becemeabundant in the strata of the Shigarami, Toyonoand Sarumaru stages, The Nishina type quartz-

porphyry and the Takase type granite are the

characteristic rock types. With the Hida Moun-tains as the main source of supply, the abundance

ratio of granitic pebbles increases as the age of

deposition becomes younger, and pebbles of ?aleo-

zoic rocks decrease. This indicates that the

erosion advanced into the deeper parts of the Hida




126

Mountains. The deposits of this period vary with

the river that transported the pebbles, and the

compoment rock types reflect the .cr.eology

o'f the

hinterland on the immediate west. Rccks in the

inner parts of thc Hlda Mottntains were net trans-

ported eut, which suggests that the Hida Mourrtainswas undergoing a west-tilting movemeiit and thc

small and short strearns on the east slde were

accurnulating the deltaic deposits.

In many cases the pebbles supplied from the HidaMountains were deposited ih the north-northeast of

the supp!y source, In the Northern Fossa Magna

some geologists attach importance to the leftward

displacement of the strata on the east ef the Itoi-

gawa-Shizuoka line (KeMATsu, 1967; KoBAyAsHi,1969). The 12-km long displacement betweenthe median dislocation line and the Yokokawa-

gawa fault around Lake Suwa has often been

discussed. (GoRAi, 1951; KAwAcHi et al., 1966),The present writer previously pointed out the

existence of an area where block movement

was active, between the Otari-Shiejiri line and

the Hakuba-Shiojiri line, and regarded this area

as part of the Itoigawa-Shizuoka line. He also

stated that the structure on the east sidc oi the

Otari-Shiojiri line was affected by Iateral pressurefrom the southeast and was warped so as to

take a nearly N-S direction (Hii{ABAyAsm, 1967,1968).

According to the writer's study of pebbles, the

distribution o,E pebbles of the Saruinaru stage,

youngest of the Neogene, is deviated 15krn north-

ward from the supplying area, and that of the

preceding age, Shigararni stage, is cleviated 30km

northward. On the other hand, the distributionof the pebbles of the Ogawa stage and older ages

does not show any unnatural deviation from the

location of their supply source. Even though the

east side of the Otari-Shiojiri line might havemade a leftward displacement against the west

side, the writer does not think the movement is

structurally important, because it seems to havecaused on!y a partial warping oi" the structure

along the line, The idea that the median disloca-

tion line was deviated and became continuous

with the Yokokawagawa fault may be acceptable,

but the writer considers that such a movement

had occurred already in the period of the base-

ment, so that the displacement after the deposi-tion of the Cenozoic system rnust be very slight,

From the above-mentioned facts, the writer thinks

that the north-northeastward deviation of the dis-

tribution of pebbles from the Hida Mountains is

attributed mainly to a river system fiowing inthat direction or to a coastal current coming frem

the south. He is inclined to think that the struc-

tural eause of the horizontal displacement is un-

lnlportant.

[t is certain that tl]esupply o[' pebbles fron], the

Hida Mountaims increasedi in the Late Miocene

Sarumaru stage when the strnctural subsidence

occurred. This agrees well with the idca hithertornaintained (KoBAyAsHi, 1957).

Even durlng the period when the Hida Moun-tains served as the major source of supply, the

pebbles of the rocks from the south, such as the

Uchirnura formation, the Sanbagawa type meta-

morphics and the Ryoke type granite, are also

founcl, though in small amounts. This fact maybe explained by assuming they are re-worked peb-bles that were transported out to be commingled

with other pebbles.

E. Period of sulu>ly of volcanic rocle Pebbges

The pebbles oi volcanic rock from the greentuff iacies of the Uchimura formation were men-

tioned before. Other volcanic rocks than these

begin to appear as pebbles in conglomerates since

the Ogawa stage, in both eastern and western

sedimentary basins. The liparitic volcanic activi-

ties occurrecl during a period from the early

Ogawa stage to the Teyono stage. The Susobana]iparite of the Ogawa stage and the Omine type

dacite of the Sarumaru stage are especially notice-

able. Andesite activities took place in various

districts since the end of the Ogawa stage, Many

of these activities were submarine eruptions d"r-ing the sedimentation, whereas younger volcanoes

of the Quaternary are found on the land. The

Omine type dacite was transported as pebblesnortheastward from the site of its activity, pro-bably due to the east-throwing movement of the

Otari-Shiojiri line. Accordingly, the Sarumaru

formation at that time must have had a fairly

wide area of deposition in both basins. The drain-

age area of the Hime River, that of the SusobanaRiver, the Joshinetsu volcanic area, thc distribu-tion area ef the Enrei formation, and the supply-

ing area of the Komoro group were the center oi

the andesitic activities which supplied large

amounts of coarse pyroclastic materials into thedepressions of vo!canic origin. In many places,

lacustrine deposits are found at the base of the

pyroclastics.

During the Shigarami stage a fresh-water en-

vironment was prevalent in the eastern sedimen-

tary basin, whereas in the western sedimentary

basin the iresh-water deposits were accurnulated

only in a very sma!1 part and the remaining partwas still under the sea until the early period of

Pleistocene, as suggested by fossils. However,



The Association for theGeological Collaboration in Japan{AGCJ)

discrimination of beach gravels from river gravelsby the shape oE pebbles cannot be made at present,because no useful clue is available.

It has been recognized by many geologists that

during the Neogene period coarse deposits rich in

pebbles werc intcrmittently accumulated in the

Northern Fossa Magna, andi along with them the

flysch-type deposits aud pyroclastic materials

formed thick beds. The writer, based on the re-

sults oi his investigation on the Neogene con-

glomerates, clarified the characters of the depositsand the geological history of the Northern FossaMagna. ALIsQ, referring to the obtained data of

geological structure, the writer was able to galnsome new facts.

E J;hrture ProbJems

As a result of this study, the following problemsremain for further confirrnation and for future in-

vestlgation,

1. Establishment of an appropriate method to

fulfi1! the requiremerits of the study en river

gravels and conglomerates. .

2. Finding an effecttve method to discriminatebeach gravels frorn river gravels, By cmploying

such rnethod, the sedirnentary environments can

be inferred from the character of gravels.

3. Similar study of fine pebbles smaller than

10rnm, and sand grains and mud, which were

excluded from the present study.

4. Study of andesite pebbles and Quaternarypebbles.

References

Hii{A[}AyAsT-aT, T. (1955) Geology of the Vicinity

of Mt, IIakuba,'Nagano Prefecture: Nagano

Prefecture Resources Investigation Association 249-262.

---

(1963) Geolegy of the San zaka Hill

along the n.orthern part of the Itoigawa-Shizu- oka tectonic line: four, GeoL S･oc. fopgn. Vol. 69, No. 813, 279-280.

-

-(1966) Provenance of the Tertiary con･

glomerates east of the Matsumoto basin, Naga-

Prefecture: four, GeoL Soc, fopan. Vol, 72, No.

4, 191-203.

(1967) Geologic structure of the northern

part of the Itoigawa-Shizuoka tectonic line:

Aid.o'ano thql17cture Edzfcation Center Reserch

Bull,, No, 1, 51-75,

---

(1968) Structaral characteristics of the

western margina] area oi the Northern Fossa

Magna : `t f;bssa J14ti.e'na," GeoJ. Soc. Jtipan, 31-35.

--- (1969) Ge61ogic structure of the Northern

Fossa Magna: IVtzfurno Proj13cture Etlzrcation

127

Cent'er Annual Roport, No. 3, 33-44.IuiMA, N, et al. (1958) Tectonic significance of

the Fossa "dagna : Earth Science (Ckileyza KZz-

gaku), g7. 29-33.KAMEi, T. (1955) Geo]ogy along the middle re-

aches of the Hime River, Nagano Prefecture: N[rg'ano thojbcture Resources lnvestigation As- sociaton, 231-236.KANEi<o, S, (1956) Asymmetric ridges in the northern part of the Ushiro-Tateyama Range :

Geogrmphical Review (Chirigufeu Hi,oron), Vol. 29, No. 8, 14-28.KAwAcHi, S. (1961) The Yatsugatake Volcanic

Chain, I, II: Earth Science (Chileyu tftJgaku),

55, 1-8, 56, 11-17.KAwAcHi, Y. et al. (1966) Crystalline schist of

Yokokawa district (Yokokawa metamorphic

rocks) north of Lake Suwa, Central Japan: lbur, R?tr. Miner, Econ. GeoL Assoc., Vol. 56, No, 1, 21-29.Ko]3.4y,xsHi, K. (1951) On the fault topography

of Mt. Jonen: Geagropical Review (Chigzifku Llyoron), Vol. 24, No. 11, 377-381.

and HIRABAyAsHI, T. (1952) The so-called

Omine Volcano and the Quaternary geologic

division in the western part of the Fossa

Magna: lbur. Geol. Soc. joPan, Vol. 58, No, 682, 293.

(1955) Nature of the Japan Alps: Tsukiji Shokan,

and HiRABAyAsHi, T. (1955) On the so-

called "mountain

boulder gravel" around

Matsumoto basin: Jbur. Geol. Soc, JlrijJan, Vol. 61, No. 712, 30-47,OMoE{i, Masae (1960) On the geological meaning

of the "Fossa

Magna": thrth Science (Chi- layu Kkxgzxleu), 50-51, 75-82.

Otari Research Group (1968) Problems in the

ncrthern part of the Itoigawa-Shizuoka tectonic

line : L`Fossa

Magna", Geol. Soc. Japan, 45-47.Saikawa Research Group (1966) Geological struc-

ture of the Sai-kawa fractured zone-Geolegy

of.'the Sai-kawa urea, Nagano Prefecture, Monograph 12, 95-102, The Association for the Geological Collaboration in Japan.SAsAKLu{A, }vl. (1932) Geelogy along the lower reaches of the Hime-kawa and structural

significance of the Hime-kawa area: flhe

IYarlh (Chikyu), Vol, 17, No. 6, 1-16.SmBA'rA, H. ancl HARA, K, (1954) Granitic rocks

from the North Alps o'f Japan (Preliminary Report) lour. (;eog Soc, .Jlipan, Vol. 60, Ne.

10, 436.4,t4,

Si-uBATA, H; and HARA, K. (1955) Nishina-type

sub-alkalic rocks from the North Alps of Japan:



The 　Assooiation 　for 　the 　Geologioal 　Collaboration 　in 　Japan 　（AGCJ ｝

128

　　 ro緲 o　 Univ．　Educ．　Res ．　RePt．　 Vol ・4，隻33−46・

TANAKA ，　K ，　et　aL （1962） On　 the　 Tertiary　system

　　 around 　 Mt．　 Moriya，　 Nagano 　 Prefecture （1st

　　repQrt ）；ノ∂％γ．　 Geol．50σ．　fapα n，　 Vo1．68，　No ．

　　 806，618−628．

　　　　 and 　HIRABAYAs 田，　T ．（1964）　 Geology　 of

　　Utsukushigahara　and 　 Sanjiro　district，　 Matsu−

　　moto 　City：　∫ou γ．　Fac．　 Educ ．，　Shinshu 　Univ・

　　No，13 ，63−79．

ToMlzAwA ，　T ．（1962）　Geological　 study 　of　the

　　Neogene　syste 皿 of 　northern 　Shinshu ： Nagano

　　Prefecture　Geological　Association・

YABE ，　H ，（1918）　Itoigawa −Shizuoka 　tectoniG　line：

　　Science　of　Today （Gendai　no 　Kagaku ），6，1−4．

YAMAGI ＄HI，1，（1958）　“Green 　tuff

，，　in　the　northern

　　district　of 　Ueda 　City，　 Nagano 　Prefecture ：

　　Treatises　in　 Co 皿 rnemoration 　 of 　 Prof．　 Haru・

　　yoshi　Fujii皿 oto’s　Sixtieth　Birthday，245−250．

YAMAsHITA ，　N ．（1960）　Alpine　 orogeny 　in　Japan

　　and 　proble皿 s　of　green　tuff　age ；Eaγth　Science

　　（（）hileyu　K αgaku ），50−51，9−21．

　　　　　　（Received 　March　27，1970）

（摘要）

中部日本，北部フォッサ・マグナの新第三系

　　　　　　礫岩と新生代地史

平林照雄

　北部フォッサマグナは，中部日本北部において，日本

列島の地質構造単位として，きわめて重要な意義をもっ

ている地域である．海退期に伴う前期中新世以降の新生

代の地層が広く分布しており，全層にわたって礫岩層が

よく発達している．しかし，この地域の堆積物，特に礫

岩について 7 全域的に，かつ長い地質時代を通して，系

統的lcVF究されたものはない．そこで，筆者は堆積物中

の礫岩の礫を用いて，後背地と堆積盆地との問の構造運

動を考察しようと試みた．

　礫岩の測定方法には種 a あるが，この研究の目的から

考えて，結果的には，長径 10mm 以上の礫を対象とす

る便宜的な方法を設定した．調査地点は 104個所におよ

び，礫の岩石種・礫径・円暦度・風化の程度・膠結物，

礫岩層中の最大礫・被度・淘汰度・走向傾斜・堆積構造

について調査した．これらの結果を検討し，礫岩の性質

からみた北部フォッサ・マグナの地史的発達を考察し

た．すなわち，後背地からの礫の供給と，堆積地域との

関係は，古い時代から新しい方へ，次の各段階に区分す

ることがでぎる，

　 1，南方の木曽西南部や，赤石山脈・伊那山脈から供

給された時代，

　 2．主として，北部フォッサ・マグナ内部の南部の内

村累層から供給された時代．

　3．1 と 2 の地域および西方ないし，西南方からの供

給時代．

　4．主として，西方ないし西南方の飛騨山脈方面から

供給された時代，

　なお， 3 と 4 では，堆積時の火山噴出物が混入し，構

成礫種に特徴をつけている．

　このような後背地の隆起・侵食運動と，堆積物との関

係の究明から，北部フォッサ・マグナ堆積盆地の構造発

達に関して，従来の研究結果の裏づけをしたり，また，

新しい知見を加えることがでぎた，特に北部フォッサ・

マグナ内部の中央隆起帯の発達や，糸魚川一壌尻線地帯

の構造発達過程と，礫の供給状況との関係を明らかにす

ることに役立った，とりわけ，従来も一

般的には考えら

れていた北部フ ri・

ッサ・マグナ地域と、その西側の飛騨

山脈との顕著な構造的対立の時代や運動が，中新世末か

ら鮮新世初期，および，鮮新世末から洪積世前期であ

り，これが飛騨山脈の急激な隆起現象によって表現され

たものであることを確認することができた．

N 工工一Eleotronio 　Library 　



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conglomerates the northern fossa magna …

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