Tertiary Depositional Pattern of Java

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PROCEEDINGS INDONESIAN PETROLEUM ASSOCIATION

Sixth Annual Convention, May 1977

PRELIMINARY STUDY

ON

THE

TERTIARY DEPOSITIONAL PAlTERNS

OF

JAVA

F.X.

SUJAN

YANTO R SUMAN

ABSTRACT. The tertiary basinal areas were developed

as a result of the interaction of the India-Australia

plates

and

the Pacific plate which formed zones

of volcanic belt, back deep and stable craton which

can be seen from South t North.

The depositional patterns show various pheno-

menas such as growth faulting, regional platforming,

flysch like deposition on trough, reef

growing

on

volcanoes, turbiditic-sliding@ding dem entation.

The patterns took place in five major regional

structural units, namely Seribu Platform, North Java

Hinge Belt, Bogor-Kendeng Trough, Axial Ridge of

Java and Southern Slope of the Axial Ridge of

Java (Lemigas

1972 .

Due to the variations in the rate of subsiden*,

supply of sediment t o the basin, local as well as

regional uplift, the sediments that filled in the

basinal areas varied considerably in the pattern of

deposition. The pattern

governed

the variation of

sediment thickness and its lithological assocation.

INTRODUCTION

General

Although Java is not the biggest island of

the Indonesian Archipelago, it is the best

known from geological viewpoint. The first

surveys were made by Jun un in 1854

and then by Verbeek Fennema in 1896

in a more complete treatise.

In the year of 1928-1941 the Geological

Survey

of

the Netherlands Indies did surveys

in some areas. Only eleven ou t of 150 planned

sheets were mapped and issued. However,

other fieldwork has also been done giving a

general geological insight of the island.

in North East Java) on the areas of

oil-oriented interest.

After a long period of inactivity,

late 1960's the surveys were resume

became more and more active in

early 1970's. Most of the surveys were

out

by oil companies (White

Shield, A

ICSI

and Shell in the offshore area

Pertamina o n shore) which carried o ut in

exploration activities including geoph

surveys, field studies and drilling program

During the period 1967-1976 at

145 wells were drilled in the Java Sea

27

wells in onshore Java (mostly in

West Java and few in North East Jav

four wells in the Madura Strait, Indo

Ocean and Sunda Strait. In addition

40,143 miles (64,590 km)

of

of

seismic were shot and 8,234 miles (1

km) were recorded on land. Ahbone

netic surveys and gravity measure

were conducted on the island by Per

and the Geological Survey

of

Indone

magnetic survey was also done by

covering the offshore part of Sout h C

Java. Those comprehensive data, al

they are sometimes contradictive, give a

step forwards in making the geologic

thesis of the area.

Pertamina, who is explpring on Jav

the greatest interest

in

knowing what b

subbasinal configurations and depos

systems exist as to eviluate the hydro

potential

in

the area.

In 1949 van Bemmelen made a comprehen-

Acknowledgement

sive compilation using all available survey

data and also incorporating data from Dutch The authors wish to thank the Mana

© IPA, 2006 - 6th Annual Convention Proceedings, 1977Disc Contents

Contents

Search



1x4

grat i tude to col leagues in the Explorat ion

Depar tment for thei r valuable cont r ibut ions,

suggestions and discussions.

GEOLOGIC SETTING

In a broad tecton ic set t ing, Java is t h e

southern smal l par t of the present Asiatic

Plate. An axial volcanic range, trending east-

west , makes up the land area represent ing a

magmat ic arc paral lel to an act ive subduct ion

zone ( t ren ch) located in the Indonesian Ocean.

The Indones i i n Ocean covers t he t r ench

( located about

250

k i n f rom t he sou t h coas t )

and most of th e non-volcanic arc.

Java holds the s t i l l emerged por t ions (now

cnd er process of submerge) of th e inner deep

to

t he sou t h o f t he vo l can i c r ange and t he

foreland basin t o th e nor th . T he Java Sea

and t he a rea t o t he no r t h i s an i dea l exampl e

of the foreland basin and shield .

From the geological point

of

view, the

Java Te r t iary basinal areas are thus n ot pro per

b a s i n s b u t r a t h e r g e o g r ap h i c al l y l i m it e d

features which are par t of a more comprehen-

sive basin including the whole Java Sea, the

sou t hern par t o f Kal i man t an and Sou t h

Sumat ra (F i gu re

1).

Lemigas i n 1969 and 1972 made separa t e

studies on North East Java basin and West /

Cent ral Java basin , the resul t indicated some

differences

in

t erm of s t rat igraphical sect ions,

l i thologies and st ructural pat terns. Never theless

using the data and combined wi th our present

knowledge, Java can be devided in to 5 maj o r

st ructural uni t s (Figure

2

f r o m N o r t h t o

Sou t h :

Ser ibu Plat form is character ized by th in

( less than 700 metres) deposi t s over ly ing

the shallow pre-Tertia, y baseme nt. This

area i s located in the nor th west corner

of

the i s land and

is

capped by Karang

Volcano.

North Java

Hinge Belt

is

an i n t e rmed i a t e

fea t u re be t ween t he p l a t fo rm and t he

basinal axis of Java. Physiographically, i t

is expressed by an alluvial-covered plain in

North West Java and by l ow

hills

in

No rth East Java. Th e sedime ntary cover

Bogor - Kendeng Trough is conside

the deepest por t ion of the basin .

area is typically capped by active vol

along the axial par t of Java. The se dim

sect ion i s made up of a huge th ic

of shaly and fiysch-like deposits.

est imated the sediments at tain a th i

of m o r e t h a n 8000 metres.

Axial Ridge-Flexure i s a narrow dis

zone bounded t o t he no r t h by an eas

trending regional flexure. This unit

sents the oldest exposures in the

and consis t s of several hg h and low are

South ern s lope of Axial Ridge-Flexu

an area a long t he sou t h coas t . The

is character ized by s outh dipping sed

of commonly carbonates .

TECTONIC AND BASIN DEVELOPME

The area under d iscussion

is

par t

Western Indonesian Archipelago consist i

three major i s lands namely Kal im

Sumatra, and Java.

In

a broader set t in

area

is

t he f ron t a l par t o f t he As i an

interact ing wi th two other major p late

Pacific plate

n

t he eas t and t he Aus t

in t he sou t h . (Kati li , 1974 ; Sukendar , 1

In th is respect t he Asian-Australian in ter

is t hough t t o be more domi nen t com

to other in teract ions when discussin

ter t iary basinal development

of

Java.

T h e oceanic-cont nen t a1 plate s co

occur red du ri ng t he Cre t aceous to Olig

(Figure 3) and exh i b i t ed a subduct i on

whi ch sh if ted sou t hw ard w i t h t he t i me.

Within the Middle Cretaceous - m

Eocene t he subduct i on zone was t r e

east -west in the area of cent ral Java and

nor th-eastward across East Java to th e

east corner of Kal imantan. To ward t he

t he zone ben t no r t hwes t ward t aki n

posi t ion of the west s ide of the Su

coast l ine. La ter on , l ikely in gradual m

t he subduct i on zone sh i f t ed sou t hwar

in

the late Ol igocene was located i

Indonesian Ocean. Th e shif t ing con

dur ing Late T er t iary and has a present po



Stratigraphy in North Java Hinge Bel

The oldest tertiary rock is the Jati

Volcanics, dated as Paleocene-Oligocene

lying the pre-Tertiary rocks. No time

exists, with the exception of in the low

section. The stratigraphy of the b

characterized by some carbonate

especially in Nor th East Java. The rem

units are mostly

of

typical shelf de

Stratigraphy in Bogor-Kendeng Troug

The stratigraphic sections here are di

compared to the area of the Hing

Flysch deposit and sediment gravity

are very common. The oldest rock

area is found in Karangkobar are

according

to

van Bemmelen is of E

age. However, whether the outcrop

situ or not is still argumentative. Th

be discussed later. In some places esp

sections below or above the flysch

some carbonates are developed.

Stratigraphy in the Axial Ridge an

Southern Slope.

In this paper the stratigraphy o

both’ areas is not separated, because the

Ridge

is

actuaIly only a part of the so

slope which underwent maximum tilt

is for this reason that almost complete s

can be measured

in

the field pre-T

Quartenary). The Axial Ridge area

part of Java where the oldest roc

outcropping. The stratigraphy depicts

structural units as the area of man

breaks, erosion phases, and vertica

horizontal change of facies. Volcano

and carbonates dominate the stratigr

sequences.

with the volcanic activities. In the first phase

the volcanic belt was located in the north-

west Java and ran east-west parallel to the

subduction trend. By Oligocene time it had

shifted

to

the south in a belt located aIong

the south coast of Java Old Andesite).

With the continued southward shifting of

the subduction zone during Late Tertiary-

Recent , it is expec ted that the volcanic belt

also continued to shift southwardly. But

instead, it was moving to the north andat

present is located at the axial part of the island.

The plate interactions are believed to have

influenced basinal formation and configuration

which

is

in fact due to the existence

of

block

faultings in th e basements pre-Tertiary as

well as Oligocene basement).

The general trend of the structural units

trending east-west is thought to be a result

s

east-west and is thougnt to be a result

of the second phase

of

collision late

Oligocene), whereas fractures developed are

basement faults.

When the collision slowed down the block

portions started to adjust isostatically, The

basinal area of Bogor-Kendeng Trough, Axial

Ridge and Southern slope of Axial Ridge

indicate tho se tectonic consequences,

However, in the North Java Hinge Belt

the subbasinal configurations were formed

earlier, though the development process was

similar. Horst and grabens in the basement are

believed to have formed during the first phase

middle Cretaceous

-

middle Eocene ) or

even older.

GENERAL STRATIGRAPHY

Since there are

so

many authors, the strati-

graphy of Java consists of various terms,

subdivisions and age interpretations which in

some cases are contradictive. Some of them

are put here

in

tables and are grouped in-

to

3

stratigraphic correlations for

est

Java, Central Java and Eest Java. In each

of the table, the stratigraphic sequences are

also grouped related with their position in

the structural unit subdivision. The aim of

DEPOSITIONAL PATTERNS

This

section will discuss some T

depositional patterns which give a

view of th e patterns occuring thro

Java. The examples were selected

many depending upon the most up

and complete data available. Four

will be discussed using diagrams



186

stratigraphic terminology and age assignments,

one should not take the data individually, but

instead using them to establish regional ideas.

Deposition in North

West

Java

The basinal configuration in Northwest

Java has been described in detail by Suyitno

et a1 and Soetomo et al, as having three

main sub-basins namely C iputa t Sub-Basin,

Pasir Putih sub-basin and Jatibarang sub-

basin. These were formed between the highs

knawn as Tanggerang High in the west,

Rengasdengklok High in the n or th central

part and Pemanukan High in the east part

(Figure

7

upper).

The area is dissected by block faultings

tren din g NNW-SSE or NNE-SSW. Th e

faultings has a great role

in

forming the

sub-basins and controlling sedimentation in

the area. The sedimentary section ranges from

3000-4500 metres in the deep parts to less

than

1000

metres in the highest part.

(Figure

7

lower).

During middle Eocene to middle Oligocene

(Figure

8-I),

volcanism was active

in

t he

area

in

connection with the plates interaction

to

the south. The area was still a land mass

and underwent severe tectonics. From the

known eruptive centres (Jatibarang and

Pemanukan) volcanic material (Jatibarang

Formation) was deposited in the down-thrown

blocks. East

of

the Seribu Platform (Tang-

gerang High) conglomerate

is

found together

with tuff indicating a very active erosion

in

the west. The irregular sinking of the

grabens caused the variation

of

the sedimentary

thickness (gro wth faulting process).

At this time the basins were likely

restricted fresh water ones. Pasir Putih

and Jatibarang Sub-Basin rapidly subsided

receiving thick volcanic sediments up t o

about

1000

metres.

The

first transgression took place from

the southeast direction in early Miocene

(Figure

8-2).

At the beginning the area was

covered by shallow sea in the east and paralic

water

in

the west (equivalent Talang Akar

gerang High, from which clastics was d

and flowed t o th e adjacent sea.

At the end

of

the early Mioce

whole area was relatively stablized (

8-3 . The area west of Pemanukan

shallow platfo rm with carbo nates we

veloped (equivalent Baturaja F orma tion

eastern part was deeper marine. The

section within the carbonates indicate

the western area underwent more subsi

Tanggerang High (Seribu Platform) wa

emerged but as a very low relief area.

In the middle M iocene, followin

carbonates depositon , th e sea con

advancing (Figure

8-4

to the wes

covered the Tanggerang high. This new

gression was accompanied by tectonic act

marked by a rapid subsidence of the C

and Pasir Putih Sub-Basin. At Rengasden

a paralic sea covered th e area where l

interbeds were deposited. The max

sedimentation was found in Pasir

attaining 1200 metres (Upper Cibu

Member).

At the end of middle Miocene (bigure

the whale area again became a stable re

platform. Limestone developed in the

of biostromJes and in many places as bio

(Parigi Formation). The tectonics were

weal and th e bioherms grow u p

to 500

m

thick in shallow, clear, warm m iddle neri t

As the sea resumed its transgression

late Miocene-Pliocene the land in the

was uplifted acting as sediment source

sea floor was deepened and the carb

growth terminated. At the end of Plio

the whole area emerged with respect

geanticline forming in the south and

tinental sediments were laid down. But l

the area then did not undergo te

activity during Plio-Pleistocene orogene (

com mo nly occured in m ost of Java.). T

shown by seismic sections with n o stru

seen

in

the Cisubuh formation.

Deposition in South Central Java

This area has been discussed in



trench zone, but afterwards it was displaced

southwardly and a new continental margin

was forme d (Pupili, 1973). At th e beginning, a

paralic sea covered t he area bu t soo n th e

sea transgressed rapidly to the nor th in

Oligocene time.

A

new interaction occured

in t he Indonesian Ocean in late Oligocene and

the volcanic belt was building up along the

south coast of Java (Old Andesite). At the

time of tecton ic adjustment fo ur main fractures

developed, nameIy Citanduy, Kroya, Southern

Hinge Line and Purworejo (Figure 9). Those

fractures would affect much

of

the develop-

ment

of

the sub-basins and depositional

patterns in the area.

As mentioned above in late Oligocene

volcanic activities appeared in the area. They

were subm arine volcanoes kno wn a s Menoreh,

K a r a n gb o l o n g a n d G a b o n V o l c a n o e s

(Figure 1

0-

1

.

In early Miocene (Fig ure 10-2) a vast

transgression occured. In the nort h, a block

sank drastically and formed a big trough

(Bogor Trough). The Kebumen area was

relatively down -thrown com pared to the

Kulon Progo and Banyumas area. In addition

in

the sub-basinal area step -faults were

formed which would influence the deposition

(in the Kebumen Sub-Basin). The Karang-

bolong and Gabon Volcanoes continued their

activities and new volcanic centre s appeared

Waturanda) . In Kebumen sub-basin where

tectonics as well as volcanism were active,

volcano-turbidities dominated the sedimenta-

tions (Waturanda Fo rmations). On th e

othex hand th e Kul on Progo area w as

stabilized,

so

that reefs could develop (Jong-

grangan Limestone). T he carbonates just

developed and the volcanic prod ucts formed

earlier the n acted as sediment sources fo r the

basin in the east (Yogyak arta Sub-Basin).

In middle Miocene (Figure 10-3) the

Banyumas area become stable (Gabon and

Karangbolong). Th e Kalipucang reefs built up

on

the former volcanic bodies. East of the

Kulon Progo area was covered by an open

marine sea in which normal sediment was depo-

sited. B ut in the Kebumen area the step-faults

Second Breccia).

The tectonic resumed during late

cene early Pliocene (Figure 10-4).

highs were exposed although a new

gression occured. The reef growth

minated in the whole area. In the B

area n orth of t he Gabon High, a n

trough was formed into which calci-vo

t u r b i d i ti e s w e r e d e p o s i te d ( H a l a n g

mation MS-1). In the mean time,

Kebumen sub-basin deposition con

but the depocenter was shif ted

to

the

because

of

the uplif t ing

in

the nor th

beginning of t h e geanticline arching).

In late Pliocene (Figure 10-5) th e no

part was uplifted in connectio n wit

forming of Java Geanticline. This resul

th e repeated subsidence of th e Bogor-Ke

Tro ug h (as seen in wells C1-SX and M

local regression and energence occured

Progo, Gabon and Karangbolong).

exposed areas acted as sediment s

for the shallow sea nearby. However,

in the southernmost par t of the Ke

the previous system existed under

marine environment.

Deposition in Middle Central Java

The Bogor-Kendeng Trough (Figu

is

believed t o have been originated fro

Eocene-Oligocene plate intera ction s

process of continous arching up of th

Geanticline is considered

to

be the

reason of its vast sinking (Figure 12).

In la te Oligocene (Figure 13-1) th

was mostly covered by deep marine a

coast line was probably situated not

t he sou th

of

th e present coast line

north ern part of th e Karangkobar area sc

reefs (Sigugur limestone) grew on the

platform indicated that the Hinge Be

was somewhat f lat and quiet . In the so

part volcanic material, derived f ro

eruptions in th e .Axial RidgelSo uthern

is postulated

to

be deposited i n the

marine environment.

A

vast transgression occured in early-



188

of t roug h in between. Clastic and calcareous

fragments were eroded f rom the Hinge Bel t

area and the Axial Ridge, where volcanism was

dominant , consumed i t s f ine volcanic mater ial

to t he rapid s inking t rough.

F l ysh like sed i men t s (Merawu and Penyat an

Format ion) and sl id ing blocks were typical

in this respects. It is believed that isolated

block of Eocene age ment ioned as thrust -sheet

by van Be mm elen is actual ly a b lock der ived

f rom t he a rea i n t he s ou t h ( t he Ax i a l R i dge)

by th is process.

In

late Miocen e (Figu re 13-3). .he trans-

gression and tec tonism were even m ore active

in the nor theastern par t s . The condi t ions were

more compl icated as the volcanism ei ther

i n t h e n o r t h ( P e n y a t a n V o l c a n o ) o r i n t h e

sou t h (Kumbang Vo l cano) i n t roduced mat er i a l

i n t he sys t em. This is the reason why clast ic,

calcareous an d volcanic sedime nts of gravity

f l ow t yp e ex i s t i n t he a r ea .

At th e end of Miocene t ime (Figure 13-4)

the s i tuat ion changed completely . A regional

up li f t occu red i n t he sou t h and some areas

were expo sed (S outh Cent ral Java). Al though

the sea s t i l l covered the area, the sea was

much shal lower than in the Pl iocene.

In t h e no r t h (Kendal and Bum i ayu) , t he r eefs

(Tapak and K apung Format io n) bui l t up ,

bu t in t he sou t hern par t t he c l as t ic i n f l ux

suppressed reefal development.

Th e arching up of the Java Geant icline again

occured in Plio-Pleistocene (Figure 13-5)

upl i ft ing most th e area and cont in ued through-

out the Pleis tocene. The upl i f t ing was

accompanied by var ious subsidence. This l ater

cond i t i on occu red i n the area o f Bumi ayu

making a f resh water basinal areas in to which

coarse clast ics and volcanics materials from

Quat ernary vo l cano were depos i t ed . In t he

sou t h . t he Kebum en area and i t s o f f sho re

par t subsided rapidly and were covered by

a deep sea.

Deposition

in

North East Java

The Hinge Bel t in Northeast Java comprises

of tw o physiographic zones (Figure 14) , h il ly

(Rembang zones ) and l ow (Pa t i and Keni ng

st ructural forming occured in East Java,

in Northw est Java i t d idn t exis t (no

tural indica t ion expressed by seismic) .

Al though the east -west general t re

t he s t ruc t u ra l un i t s domi nat es t he pa

t he t ec t on i c e l emen t s onshore and o f

also have a nor theast -southwest t rend

Trough, Bawean Arc h) indicating th e inf

of th e older p lates in teract ion.

In t he Ol i gocene (F i gu re 15 - I ) , t h

had al ready reached the Java Sea ( t

not th e case in th e C ent ral and Wes

The Kendeng z one was covered by deep

into which volcano clast ic materials d

from Old Andesi te Volcanoes were dep

In the Java Sea area some stable shel f

were es tab li shed wh i ch con t i nued t

onshore Kujung area. In th is area r

bodies were form ed (Supar jadi e t a1

As also demo nst rate d previously in C

Java during early Miocene, as the ne

t rasngression s tar ted up, the tectonics b

very act ive (Figure

15-2).

The Nor t her

South ern Hinge Line acted o ut as the Ke

Trou gh in betw een subsided. Th e K

area became unstable so that i t w

favourable for the c ont inuat ion of reefs g

I n t h e s o u t h t h e a r ea w as b o u n d e d

ac t ive f au l t . Due t o t he ac t i v i ty of t he

t he a rea no r t h o f t h i s f au lt somet imes e

ed and t he a rea t o t he sou t h was c

by shal low t o deep sea . In t he i n t e rmi

shal low-deep sea, m ar k and c arbonates (K

Format i on ) were depos i t ed

in

the s

At t h e sam e t i me f l y sh l i ke depos i t ion o

in th e t rough (Pelang Format ion) .

In mi dd l e Mi ocene (F igu re 15 -3 )

nor thern area was upl i f ted . The Kujun

emerged and peripherically the sea sha

(ner i t ic-paral ic sea) ; towards the

(Ngimbang Well) i t was deep water m

The such cond i t i on accomodat ed a depos

sys t em i n wh i ch more c l as t i cs i

no r t h and con t r ad i c t o ry more mar l

carbonat es t o t he sou t h (OK Form

Stil l , as

in

the ear ly Miocene, the

was f i l led wi th the f lysch deposi t s

Format ion) .



previous tectonic activity, protruded as a

stable high, while the area southward was

actively deepened. Reefs Karren limestone

)

built-up o n the stable areas, whereas mark and

carbonates were deposited in the deeper

areas Lower GL Format ion). The Kendeng

Trough again underwent faulting and sub-

siding. Turbidities and slumping were its

typical sediments Kerek Formation).

In the Pliocene Figure

15-5)

the condition

changed in connection with the beginning

of t he arching up of the Geanticline and

shallowing of the sea floor in th e Kendeng area.

Ln the north area clastics and volcanic products

were deposited and locally far from the

clastic influence, reefs were able to build up

Dander Limestone). The areas to t he nor th

were more stable with an exception of

Bojonegoro area. Reefs continued growing

in the Kujung area Karren Limestone) and

the area south of this high was covered by

an open shelf sea with carbonate clastic system

of deposition Upper GL Formation).

The regional Plio-Pleistocene tectonics

occured in Northeast Java resulting in the

shallowing of t he sea in the northernarea.

I n the basin clastic sediments were deposited

MT Formation).

CONCLUSION

1. The Java basinal areas have been demon-

strated as having various depositional pheno-

menas that can be grouped into patterns

which are

in

close relation with the

structural units.

2 The trend of the regional basinal areas

were governed by the plates interaction in th e

Eocene-Oligocene. The older was responsible

particularly for the basinal development in

Northwest Java.

3 . Deposition in the Hinge Belt was marked

by shelf deposits comprises both clastics

and carbonates, Although the subsidence was

not uncommon, the ra te was equibalanced

by the sediment supplies. The trough sedi-

mentation is characterized by its greater

thickness d ue to th e rapid subsidence especially

during early-middle Miocene, Flysch-like

versed blocks involved so that the pa

change within short distances. Volcanis

its related reefs as well as sediment

flows are typical for this area.

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D., SUYITNO

P.: The Ci

Formation as one of the most pros

Stratigraphic units in the North-we

Basinal Area. Indonesia Petroleum Ass

Convention, Jakarta, 1975.

ARPANDI

D.:

Carbonates outcrops in Wes

Indonesian Petroleum Association Ca

Seminar, Jakarta, 1976.

BEMMELEN van, R.W.:

The Geologyof

sia, volume

1.4

Martinus Nijhoff, The H

1949.

BOLLIGER,

W .

RUITER, de P.A.C.:

G

of the South Central Java Offshore

Indonesia Petroleum Association Conv

Jakarta, 1975.

KATTLI, J.A.: Geological Environment

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Tertiary Depositional Pattern of Java

Documents

onshore java

north east java

north west java

java sea area

north java hinge belt

south central java

axial ridge of java

offshore areas