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
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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
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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
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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
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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-
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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) .
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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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