PERTEMUAN IlMIAH ARKEOlOGI VI~u, MAlANG,JAWA TIMUR 26--'OJUlII992

BOKO PANDOAN

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t::~6:-::-".;

SUMBANGAN ARIŒOLOGI UNTUkPERIŒMBANCAN MASYARAkATDAN IŒ8UDAYMN INOONESIA

-.

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...******************P 1A Congress VI, Malang, July'92

CHRONOLOGY AND PALAEOENVIRONMENT OFPLIO-PLEISTOCENE DEPOSITS IN THE SOLODEPRESSION (CENTRAL JAVA): THE KALiUTER AREAAND ITS RELATIONS WITH THE ANCIENT JAVANESESETTLEMENTS.

by Tony DJUBIANTONO, François SÉMAH, Anne-Marie SÉMAH

Kronologi dan Paleoekologi endapan Plio-Plistosen di DepresiSolo (Jawa Tengah): Oaerah Kaliuter dan hubungannya dengankolonisasi pertama Pulau Jawa.

RINGKASAN

A. Pendahuluan tentang seri stratigra1i Kaliuter

Depresi Solo. yang terletak di bagian tengah Pulau Jawa. diapit oleh Perbukitan

Kendeng dan Pegunungan Selatan. Daerah tersebut. termasuk lereng Selatan

Pegunungan Kendeng. yang mengandung banyak situs paleontologi dan prasejarah

terkenal, sepertl Kubah Sangiran.

Secara umum, stratigrafi yang dapat kita tinjau di depresi Solo menunjukkan seri

regresi lautan antara zaman Pliosen atas dan Plistosen tengah.

L3pisan pengandung fosil selalu dimulai dengan lapisan pertama yang berfasies

daratan.

Namun, fosil vertebrata dan manusia purba yang kita dapat di daerah Sangiran telah

diangkut jauh dari tempat hidupnya. kemudian diendapkan kedalam cekungan depresi

Solo. Apabila kita ingin meneliti tentang kolonisasi pertama Pulau Jawa oleh fauna

mammalia dan manusia purba. periu kita mencari situs yang lebih dekat dari pegunun­

gan yang telah berada pada zaman itu. misalnya Perbukitan Kendeng.

r

. u p 1 A. Congress VI. Malang, July'92 2

Dan segi itu kita memilih daerah Kaliuter sebagai daerah penelitian. Disini kita bisa

menlnjau suatu seri stratigrafi lautan dangkal yang sangat tebal, dimana perlipatannya

memberikan banyak informasi langsung tentang evolusi tek10nik Perbukitan Kendeng.

Disamplng !tu juga, di daerah tersebut kita telah menemukan beberapa situs paleon­

tologi baru, seperti situs Kedung Cumpleng (dengan beberapa artefak batu) dan situs

Pancuran (di mana ditemukan dua gigi manusia purba).

B.Penelitian Paleomagnetisma

AnalislS paleomagnetisma ternyata sangat sesuai apabia kita mau mempelajari

secara kronologis lintasan-lintasan daerah Kaliuter. Kenyataannya, lapisan pengandung

hasil keglatan gunungapi sulit dianalisis dengan metoda pertanggalan mutlak seperti

Potassium Argon. dikarenakan minerai-minerai telah mengalaml proses pelapukan

yang sangat panlang.

Beberapa zona poIariti geomagnetik purba dapat dilihat pada setiap Iintasan yang

ditellti

Secara keseluruhan, ternyata ada suatu kontradiksi antara hasil yang dicapai di

daerah Barong (paling Utara) dan di lintasan lainnya. Hal ini dapal membuk1ikan bahwa

endapan lempung biru telah mulai lebih dahulu di Soko, di Selatan daerah Kaliuter.

Hipotesa paleomagnetisma menunjukkan bahwa transisi Brunhes/Matuyama (0.7

Juta tahun) terletak di bagian atas sen lautan, pada lapisan batugamping Salanus.

Konglomerat Kedung Cumpleng dapat dipertanggalkan pada episode Jaramillo

(0.87-0.97 juta tahun), sedangkan zone positip yang terdapat pada fasies gampingan

di Soko dan di Sarong berumur 1.67-2.1 juta tahun yang laJu (episode QldlNai dan

ReunIon). Sagian bawah dari Iintasan Sarong diendapkan pada awal periode

Matuyama, antara 2.48 dan 2.2 juta tahun yang laJu.

C.Penelitian Palynologi

Analisis pollen telah dilakukan pada lintasan Soko, mulai dari lempung biru sampai

lempung pasiran diatas lapisan konglomerat Kedung Cumpleng.

Pengaruh dari hutan payau temyata sangat stabil di sepanjang Iintasan tersebut. Hal

ini sesuai dengan hasil analisis sedimentologi atas endapan Iaguna.

Lintasan Soko dimulai dengan suatu periode dimana perbukitan di sekitarnya dihuni

oleh suatu hutan hujan tropis.

•

******************P 1A. Congress VI. Malang, July'92 3

Kemudlan kita mendapatkan suatu periooe dengan penggantian antara hutan hujan

tropis dan pemandangan terbuka (rumput).

Pada baglan dasar konglomerat Kedung Cumpleng. vegetasi sekitarnya berubah

kembali menjadi hutan terbuka (iklim dengan musim kemarau panjang)

Sedangkan diatas konglomerat terdapat penggantian antara hutan hujan dan

pemandangan terbuka.

Pada lapisan lempungan di bagian atas lintasan, rumput dan pakis menladi dominan,

dan vegetasi mencirikan suatu periooe dengan kegiatan gunungapi.

D.Daerah Kaliuter dari segi Paleogeografi

Daerah Kaliuter sendiri memberikan banyak informasi tentang evolusi geologi

depresl Solo.

-Fasles dangkal ditemukan pada lapisan yang cukup tua. yaitu di lintasan Sarong

leblh dan 2 Juta tahun yang lalu.

.Pengaruh gunungapi adalah dominan pada lapisan teratas di Kaliuter. tetapi juga

dapat dilihat pada lapisan lautan yang terakhir. Ternyata bahwa pengaruh kegiatan

gunungapi terjadi lebih dufu, dan secara lebih intensif pada Iintasan Soke. yang terletak

pahng Selatan

-Di daerah Kaliuter kita mendapatkan dua bukti tentang evolusi tektenik Perbukitan

Kendeng:

1.Perlipatan terakhir. yang terjadi di sekitar 0.7 juta tahun yang lalu.

2.Konglomerat Kedung Cumpleng, yang membuktikan bahwa. pada satu juta

tahun yang lalu, Perbukitan Kendeng sudah muncul diatas muka air laut; perbukitan

tersebut sudah dihuni pada waktu itu oleh fauna mammalia serta manusia purba.

Dengan skala yang lebih luas, kita sekarang sudah bisa me~gusulkan suatu evolusi

paleogeografi yang meliputi daerah Sangiran-Kaliuter.

*****"*""U'U*****P 1A Congress VI. Malang, July'92

A. AN INTRODUCTION TO THE KALiUTER SERIES

by Tony DJUBIANTONO, François SÉMAH, Anne-Marie SÉMAH

I.The Solo depression

4

The Solo depression, ln the centre of Java Island. is filled by large volcanoes and by

quaternary alluvia. It is limrted by the Kendeng hlll range northwards, and by the

Southern Mountains of Java.

Many Important fossll-bearing sites are located within the depression or along the

southern flank of the Kendeng hills, like' Bumlayu. Sangiran. Trinil. Kedungbrubus and

MOlokerto (Fig. 1)

As a bulk. the stratigraphical series we find in the Solo depression glVe the plcture

of the recesslon of the sea during the Upper Pliocene and the Pleistocene.

II.The Sangiran-Gemolong series

We shall recall briefly here the dasslcal stratigraphical section of the Sangiran ­

Gemolong area, near Solo town (Fig. 2).

The section begins with open sea pliocene deposits, the so-called Lower Kalibeng

Globigerina marls. The recessive facies appear during the Upper Pliocene, as blue c1ays

deposited in a lagoon (Upper Kalibeng beds). Pollen analysis (A.-M. Sémah, 1986) show

that the lagoon was bordered by a large mangrove forest formation. These recessive

facies appear at about 2.4 m.yrs ago in Gemolong, and persisted until the Plio-Pleis­

tocene boundary (F. Sémah. 1986).

Then we find volcanic breccia dated at about 1.6/1.B m.yrs, which yielded the oldest

vertebrate remains found in Sangiran (LJ.C. van Es, 1931), followed by the deposition

of the thick fossil- bearing Pucangan days -which already contain fossil mammals and

homlnids.

The top of the Pucangan unit consists of a conglomeratic fossiliferous layer. named

Grenzbank (G.H.R. von Koenigswald. 1940). This layer is dated between 0.7 and 0.9

m.yrs aga (see F. Sémah, 1986; N. Watanabe and D. Kadar, 1985).

Complexe de Idjen

.Â

Détroit de Madura

100 kil)

..G Wilis

Kedungbrubus MojokertoButak

Kalluter

• SangiranoSolo

G. Merapl

• Les Collines de Kendeng

Il Monlagnes du Sud

~ '- '""" '-'UPPER GRAVEL (

M YRS ~o'-.....;o, -

v": ,,

NOTOPURO VOLCANICS: ;:5 ' ', -, -

KABUH ,ALLUVIAAND TUFFS

c -; 08 •••• -..- GMEN28ANK

PUCANGANCLAYSISWAMP)

6

, 5, 1 7

2 4

VOLCANIC BRECCIA

UPPER KALiBENG

CLAYS & lIMESrONE(LAGOON\

LOWER KAUBENGMARLS(OPEN SEA)

AG. 2 SYNTHETlC SECTION OF SANGIRAN/GEMOLONG AREA

· .. ·············***P 1A Congress VI. Malang, July'92 7

But the greatest number of mammals and homlnids are found in the Kabuh volcano­

sedimentary senes. dating back to the Middle Pleistocene. One of the sites we presently

excavate. at Ngebung, in the Sangiran dome. yielded severai stone artrfacts (F Sémah

et al , 1992).

At the upper part of the section we find the Notopuro breccias and lahars (ca. 0.25

m yrs, M. Suzuki et al.. 1985), and younger alilNial formations.

III.The interest of the Kaliuter area

Whatever the site we choose in the area. the oldest continental mammals appear

wlthln the first continental layers. If our interest focuses on the older Javanese settle­

ments. it is therefore very important to study the last manne deposits, which precisely

pre-date the colonlzatlon of Java.

Volcanlsm. tectonlCs. and especially the emergence of the Kendeng hills were at the

ongln of the recesslon of the sea in the Solo depress/on.

At Sanglran, we observe that mammals and hominid fossils are heavlly rolled. and

have suHered a substantial transport far from their habitat. Loglcally, this habitat has ta

be searched for nearer to the older reliefs which were already emerged at those times.

Sites which are located near the Kendeng hills are therefore Iikely to provide us with

Important information about the older settlement, and about the plio-plelstocene tec­

:oniCS ln the area.

This was the baSIS of our interest to study the Kaliuter area. on the Southern flank of

the Kendeng hills. 30 km North of the Solo town (Fig. 3).

This area presents several advantages:

-we find there thick shallow marine deposits. in the form of continuous stratlgraphical

sections.

-from the tectonical point of view, the Kaliuter area is directly Iinked to the Kendeng

hills, it is therefore definitely different from other sites like Sangiran. whose folding was

Ilnked with other phenomena (for instance diapirism).

-we discovered severa! new fossil-bearing sites near Kaliuter.

1

1

Riv.SERANG1

10 km

N

8

• COWNES DE KENDENG

• KAIJUTER

FIG. 3 LOCATION OF KAlIUTER AREA

.'

..................p 1 A Congress VI. Malang, July'92

IV.The Kaliuter series

9

LoUIS Jean Chrétien van Es. a Dutch geologist. described in 1931 the stratlgraphical

senes of Kaliuter and carried out complete geological mappmg. Sut he dld not mention

the occurence of fossil mamma/-bearing layers. The map given on Figure 4 IS drawn

from van Es' one, and completed by our own survey concermng several important

stratlgraphical boundaries.

We shared the stratigraphy between three parts:

-The folded series. mainly of marine character, which show a Southeast dipping

linked to the Kendeng tectonics.

·The transltlonal series, contemporaneous of the folding event.

·The hOrizontal series, which postdate the last folding event.

Our stratlgraphlcal work focused on several sections, the most Important concernmg

the so-called folded serles:- Sarong, Soko and Kedung Krujuk.

IV. 1. The folded series

At Sarong (Fig.5l, at the basis of the section. we find the classical G/obigenna mans,

deposlted m an open sea environment These layers are covered by shallower deposrts,

Ilke sandy c1ays which contain charceals. leaves and seeds, fish and mollusca remains.

and sometlmes amber fragments. Higher we find banked limy layers with littoral

mollusca and sea urchins. A cmeritic layer is found in this part of the section, which ends

bya clear contact with a fine-grained blue clay unit.

Along the Soko section (Fig. 6), we find first a yeHow limestone with coral reef

fragments, then the banked limy layers with mollusca. sea urchins and wood fragments.

Then we have a more sandy layer. which contains a large amount of volcanic minerais.

It forms the boundary with the b1ue clay unit.

The blue ctays are very uniform. In their upper part, they show several oxydized

sandy banks and thin cineritic layers. They end with a consplcuous deltaic conglomerate

at Kedung Cumpleng, deposited in a coastal environment.

This conglomerate contains limestone pebbles. mollusca. corals and Salanus. Some

rolled mammal bones are likely to be found here.

Then we find sandy clayey layers with fossilized trunks, a cineritic bed and again the

blue clay facies.

-

-o

, ..

l ,,1 III Il i

1 Il 1 l ,1 Il' 1111

Il i i 1 1 1

_ l , Li 1 1 1 1 _ 1..

Il 1 Ji 111:11 Ji ~']I IL

1 1

,1 Il Il 1

FIG 4 GEOLOGICAL MAP OF KALiUTER

,,1 Il j Il 1 f

i 1 1 Il

, \ 1 l ,\ II· -[

,',11 , 11 1 1;1 1 1 Il

1,1 1 , 11 1

r 1, Jill

1 III Il 1

1 1 II Il ,1 [Jf W l 'i~ 1 IlL Il II 1 1·' 1

IL,I r Il

1 j

o~~

~

LUoo

oo

\.' '/ \

,ç..,1 ',; \' \ J .,

\' \' \ l " \,' './ ,/ '.

1--­1--­~-­

1- - .....KO 516

11

~--1- .. _ .. -"'-"'_" __-:-:..--:.:..-::..-.~-~

- - _. - _. -K05101- - _ - _.-:':" .E-:.-j AAGILE BLEUE

t~~~.~j ARGILE SABLEUSE I~K0498

KO 14()

~ CALCAIAE uTE

f-KOSO

....K030

K0130

0120hl~·· 1.1

KO 110

-,0- - ---= o~o-

1- -

'- - - - - ~KO 701------ - - ,1-. ­

'- -- -1--_ - _ - _ -_ - ~K060

---. - .......l--- _ - 1'"""\-

1--­

--~

---1-. -

1-- -1-- -1--.:---_.I-~- 0 -0-·

- ----1- ­--:--1---~ .. -. _. _. -1-= -:-= -=:"-=.-: ~0201- .. - _. _. -' .

:=5~.:,,-D=== ..~. -. - .. -' -·-K01O~-=:-:~-:- .7J~.:.:. !?--:"~. ;'0 -'. ''2)'' -'0- '-K01

~ CALCAIAE LITE '(Fos$.ll8$lrtorauxl

III AAGILE SABLEUSE

E.::.=.;·~ AAGILE SABLEUSE A MOUUSOUES

FIG. 5 THE BARONG SECTION

- - - --- - - --J-KU163~----- .

- -- -

---~ - _ - _ - _ -_-_-I(Ul60

- - - - - . -SAM 1~ - - - - -

~ - ~ ...:.....:.... -I-KUI40- - - <ô -- - - --~- -@. - - -- -- Q- -Q -.- -6- - -_ G - - - _ ....K U 130_ ê_

f-O.-'0-'.-.~"""'."""".'.•:-""-~~M·"'.~-.•- ...-I-KU 125KU 124

- --SAM 21

12

E= =~ ARGiLE

E-t.:...i:-1 ARGILE SABLEUSE (C1nenle. moIl~ DOIl

Ei-~ ~.j ARGILE SABLEUSE ibolS el mollUSQues'

(~~~t3 CONGLOMERAT FOSSllIFERE

~-_ --1 ARGILE ôABLEUSE (Clne,Rel

~-­

~-­

~-­

~ ­~---

- -- -

~KU 100

t----1 ARGILE 3LEuE

r- -~---

~-­

1- ­1----1---

1- ­1-- -

'-KU 90

--KU 80

... 1 ~l

"'KU60

1- - ---- -1-- _ - _ - _ - =- I-K U 70~--

.->-- ­.--­1---

~_-_-_-_-=--K i.J 50

1- -

I-KU40

-KU20

KU10

KUI

FIG. 6 THE SOKO SECTION

[ '0 m

......................p 1 A Congress YI, Malang, July'92 13

At Kedung Krujuk (Fig. 7), above the b/ue clays, we have cinerrtic banks. coastal

limy sands and a very sandy conglomeratic layer which contains fossll mammals. The

section ends wlth a thlck Ba/anus limestone. the last marine layer whlch has a large

extension ln the area.

IV.2. The transitional series

The transitional facies, showing very irregular dippings, cover the Balanus lime­

stones. These layers have undergone a tectonic influence. They conSlst of blue c1ays,

clnerrte. black clays and Iignitic deposits with leaves and wooo. We find also limy sands

wrth molluscs. Ba/anus and sea urchins. The sands are often cemented, showlng fossil

dunes and beach surfaces, with a lot of fosstl trees.

IV.3. The horizontal series

Any manne Indication lacks from the horIZontal series. which are charactenzed by

fluviatile cross-bedded sands, tuffs and at the top by volcanlc breccla of reglonal

extenSion The sands contain a lot of mammal fossils. Including a complete Stegodon

jaw found near Kedung Kancil.

The Kaliuter stratigraphy ends with deposrts which postdate the eroslon of the hilis

by the river' alluvial terraces and travertines.

V.Archaeological excavations in Kaliuter

Since 1989, the whole of the area is covered by the Kedung Ombo dam lake. In 1987

and 1988, we organized excavations in order to collect data about the main sites which

have disappeared now.

The Kedung Cumpleng excavation has been carried out in the deltaic conglomerate.

It yielded mammal fossils Iike Stegodon, Rhinoceros, bovids, cervids et suids. We find

also crocodile teeth, bones of tortoise. shark teeth and other fishes. Several bones

have completely disappeared, and are replaced by their concretionated limy mold.

Many limestone pebbles are broken, and some pieces have been worked out by

man. Among these items are several very fiat flakes, and bifacial tools (Fig. 8, 9 and 10).

The Pancuran site belongs to the horizontal series which postdate the folding phase.

It shows coarse flLNiatile sands below the volcanic breccia. These sands contain a lot

of fossil mammals like E/ephas, Rhinoceros, cervids. bovids, suids. and also a

cercopithecinae tooth.

~_~_g§_~_~_~~_~rI';U 524 -SAM A- _. -

14

- .'-.

U523 -SAMD

KU 522

U621

~ ;: ::i:i: :;l CALCAIRE ~ 3AL4NUS

t=-=:.-==J MARNES SABLELJSES)

t~~~~l CONGLOMERAT

~ CALCAIRE SABLEux

l';U 517

U516

KU 515

KU 514

KU513

f~~:~~:~ ARGILES

~~;=~!:] ARGILE3

9BLEUSES\

- _.. - - ------ -- --

U 506

U 502

U 501

KUSOO

FIG. 7 THE KEDUNG KRUJUK SECTION

FIG 8 KEDUNG CUMPLENG FLAKE (drawing H Widianto)

i"'-

f 3cm

'4"...

FIG 9 KEDUNG CUMPLENG FLAKE (drawing H Widianto)

•

4 CM

FIG 10 KEDUNG CUMPLENG STONE TOOL (drawillY 1-1. v~,.liJnlo)

'.

,,,,,,,,,,,,,,,,,,,,,•••••••p 1 A Congress VI. Malang, July'92 18

Many of the bones are still in anatomlC connectlon. The animais were killed lust alter

a volcanlc eruption, as the SinUS of a young elephant skull are covered wlth cemented

voleanlc ashes.

The Pancuran site Ylelded also the first human fosslls discovered in the Kaliuter area.

. e a molar and an InClsor.

B.PALEOMAGNETIC STUDY OF THE KALiUTER

SERIES

by Tony DJUBIANTONO

I.Paleomagnetic analysis

1. 1. Methodological approach

Java Island is situated within a strong volcanlC enwonment, but it is still diffieult ta

date by geoehronologlcal methods the volcanlc effluents Intercalated in the quaternary

fossil-beanng deposlts

Indeed. these volcanlc effluents are very often weathered volcanle ashes. which

cannot be easlly analyzed by means of Potassium Argon method. On the eontrary,

paleomagnetic analysis have given very important results on several stratigraphical

senes in the Solo depression. The thick KaJiuter sections are very suitable for such a

research.

From a methodological point of view. our palaeomagnetic analysis on the Kaliuter

sed iments used a thermie attack of the viscous remanent magnetization (VAM) in order

to get the direction of the primary detrital magnetization (DAM). The thermal attack has

to match relaxation times of ca. 1 m.yrs before we can consider the obtained polarity

wrth enough certainty.

The results we present here take the shape of angular distance to the present dipole

field. This distance is zero for a pure normal poIarity, and 180 degrees for a pure reversed

polarrty.

. *****""""*"""*""""P 1A Congress VI. Malang. July'92

1.2. The Barong section

19

•

The 371 specimens of the Barong section first gave very scanered directions But

several zones of magnetlc polarrty appear dunng the analysis. descnbed as follow (Fig.

11 )

·At the very basis of the section. a reversed zone followed by undetermined polantles:

·Then a reversed lower zone;

·An Intermediate zone where normal polarities are dominant. But thls zone IS cut by

an undetermlned one and bya reversed subzone.

·in the upper pan. a somewhat thick reversed zone.

'Jn the straligraphlcal representatlon (Fig. 12). we notice that the normal pOlanties

jlsappear at Barong ln the mlddle of the banked limestone facies. weil below the contact

Nlth the blue clays.

1.3.The lower Soko section

The tlrst measurements of the 214 specimens of the lower Soko section share them

Detween a lower normal zone and an upper reversed one. The contrast becomes

st ronger after the thermal analysis (Fig. 13). The upper reversed zone gNes very grouped

"esults It beglns just above the lower boundary of the blue clays (Fig. 14)

1.4.The upper Soko section

ThiS section. Including 82 speCimens. directly follows the lower Soko section. The

natural magnetization diagrams are hard to interpret. but the statistic means after

thermal treatment glve c1ear results. The section is shared between three zones (Fig. 15

and 16)

-The lower pan. with blue c1ays. is reversed.

-Just above the Kedung Cumpleng conglomerate, normal polarrties are dominant

-Reversed polarities are found again in the upper pan.

1.5.The Kedung Krujuk section

The study of 48 specimens gives two zones on this section after thermal anack (Fig.

17and18)'

20

specimens

1

..~ 100~s

il ~

~ 350,- "~-4>a.

"'"..uCIl

"t:T 300~.,

r1 ~

250

li J~::::::--1.. 1

-=:::::;-ë...,

200~..uCQI

" -it:T-4>

'" 11

150

18090

cDUCcD

"t:T~ 0 +--.--,-r------.--~----r-.______r___r_____r-,___r_____r___,-...__..,___r____i

a+

FIG. 11 SARONG, PALEOMAGNETISM

- - - - - - - - - - -

- - - - - - - ~ - - -

- - - - - - - - - - --- -- _.- - - --- - - - - - - - - - -

: : : : : : : : : : :

- - - - . - - - - - -

:::::::::::

:::::::::::

---------~.

- - - - - - - - - - -

- - - - - - - - - - -:::::::::::

:::::::::::

- - - - - - - - - - -

<:

1-

::::

1

21

FIG. 12 SARONG, PALEOMAGNETISM vs. STRATIGRAPHY

22

specimens

200

C>

~ 150~

~C>

'"

100

50

18090O-+-----.-----,r--..,..----.--r--..,..-----.--~__r____.-__r____,_____.-__r____,_____.-_r_____l

o+

FIG. 13 lOWER SOKO, PALEOMAGNETISM

- - - - - - - - - - -

rML.ta~'"~~--.---------------------. - - - - - - - - - -

-

:-:-:: :::::-:-:-- -

- - - - - - -- - - - - - - -

23

- -- - - - - - - - - ­. - - -- - - - - - - - - ~ -

-----------------------

-------------------------------------------------------

-' --------

-',

-

FIG. 14 LOWEA SOKO, PALEOMAGNETISM vs. STRATIGRAPHY

24

FIG. 15 UPPER SOKO. PALEOMAGNETISM

-"'1 ('1/-"':" l'

.....,Ii \-1 \..1

25

FIG. 16 UPPER SOKO. PALEOMAGNETISM vs. STRAllGRAPHY

26

50,...--------------:-----------~

Î

II>UCII>::JCT~<Il

40

35

30

1

25

II>

::J 20!!~C

II>UCII>::J

15cr-4><Il

10

5

1890O+--.---.......,----.--.-----,--,-~~-+---r---r___r-r__r__r___r__r___l

o+

FIG. 17 KEDUNG KRUJUK, PALEOMAGNETISM

-

-

-

,--

f--------------1

------------

27

FIG. 18 KEDUNG KRUJUK. PALEOMAGNETISM vs. STRATIGRAPHY

****"'*****"'*******P 1A Congress VI, Malang, July'92

·reversed polantles ln the lower part,

28

·a clear and graduai change to normal polanties at the top of the section, ln the

Balanus Iimestones

II.Chronological interpretation

11.1.Lithostratigraphy vs. magnetostratigraphy

If we conslder pure Iithostratigraphical correlations between the studied sections.

we see that the accordance between paleomagnetlc results IS good for Soko and

Kedung KrulUk sections, which are almost sltuated ln contlnUity in the field (Fig 19)

The banked Iimestones show a normal polanty, then we have a long reversed zone

in the blue clays A smaller normal zone appears above the Kedung Cumpleng con­

glomerate and then we flnd again reversed polarities till the last tranSition in the Ba/anus

Ilmestones

But a contradiction eXlsts wlth the Barong section. The lower normal zone ends ln

Soko at the very basls of the blue c1ays. and much earlier in Sarong, wlthin the banked

Iimestone facies The dlfference IS approxlmately 50 meters

1n order to correlate the palaeomagnetlc data, we have therefore to shlft up or down

the Barong section. The upward shlfting IS more satisfying because (Fig. 20)

·It places ln the same geomagnetlc zone the reversed polarities found at Barong and

at Soko.

-It IS ln good accordance with the cartographlc results which show a wedglng out of

the blue clays northwards. This is obvious on the virtual geological map (Fig 21) where

ail the area. with a constant dipping, is represented at the same altitude.

We may therefore assume that. when the blue c1ays already deposited at Soko,

calcareous sediments still deposited at Barong.

11.2.The chronological model

Several hypothesls can be glven for the chronological interpretation of our

palaeomagnetic results. The uppermost reversed-normal transition could be attributed

to:

-the basis of the Olduvai event (hyp. TA)

-the basis of the Jaramillo event (hyp. A)

Z9

K. KRUJUK

SOKO SUP

~

~

- 1-i·i·llf·C ~ .

SOKO INF.

v>Ql:JQl

15v>

~Cl>;;;v>

'"TJca

'"a.a.

'"• •

-.--

FIG. 19 L1THOSTRATIGRAPHICAL CORRELATIONS

1SARONG

BARONG

1

cgtaa.a.ta

SOKO INF

~«

:;:.(

~

i":' 1SOKO SUP.

K. KRUJUK

30

FIG. 20 PALEOMAGNETIC CORRELATIONS

": ~_' '-- 1

FIG. 21 VIRTUAL GEOLOGICAL MAP

"1

CiCUJ

*"u**uu********p 1A Congress VI. Malang, July'92

·or the SrunhesjMatuyama boundary (hyp. R)

32

The first hypothesls can be discarded. as It would implya Gauss age (more than 2 5

m yrs) for the Kedung Cumpleng prehlstonc site. This IS ln contradiction wlth our present

knowledge about older javanese settlements.

The second one would imply an Olduvai-Reunion age for the Kedung Cumpleng site

(ca. 2 m.yrs ago). It is extremely old, but not completely impossible.

Nevertheless. we presently choose the third hypothesis for several reasons:

·The palaeomagnetlc analysis carned out in the upper horizontal series did not show

reversed po/arilles. These series are likely to be related to the Brunhes chrono

-The sedimentation curves drawn are closer with the one of Sanglran-Gemolong ln

the case of thls "youngest" hypothesls (Fig. 22).

Our model (Fig 23) relates therefore the Kedung Cumpleng conglomerate to the

Jaramillo event. This age represents a minimum age for this prehistonc site

The normal sequences found in the Sarong section are related to the Olduval­

~eunlon events (1 67-2 1 m.yrs). It is not strange to find reversed sub-zones ln such a

complex geomagnelic penod. A more complicated geomagnetic figure was descnbed

in the Omo valley sens by R.T Shuey et al. (1974)

The reversed zone found at the bottom of the Sarong section dates therefore back

to the beglnnlng of the Matuyama chrono between 2.48 and 2.2 m.yrs ago

3000

[~J

2500

2000

1500 //

[~]

~ //

, rSANGIRAN / GEMOLONG 1

1000

IARGILES BLEUES 1

500+------,-,--~====;,=====-------.----------.----------io 50 100 150 200 250

FIG 22 SEDIMENTATION CURVES (Ilyp R vs SangiranGemolong)

ww

-

,. u

"

11

J]

Ci)

1\) w () I ::c 0 Z 0 r 0 G> ë) »- r ~

10 0

[\)

III

m r(_n

)

-,',.}

-.:>--

!

1Il

III

l'.

;l1

Il

\,

'1

o o

Il

" "oj

'': o

TI

1r

11r

ifIl

.******.... *******p 1A Congress VI. Malang. July'92 35

C.POLLEN ANALYSIS Of THE SOKO SECTION,KALiUTER

by Anne-Marie SÉMAH

I.The Pollen diagram

The polllnic study of the Kaliuter area focused on the Soko sections, beginning wlth

the blue clays and ending weil above the Kedung Cumpleng conglomerate.

The polltnic diagram shows a lot of different arboreal elements. The tree percentage.

as observed ln Figures 24 and 25. is higher than the herbaceous one -except for smaller

oscillations-, and similar to the fem frequency.

Many taxa are regularly present in the basic diagram. Among the trees. the

Arecaceae. and especially Nypa fruticans; Casuarina, Excoecaria, the Fagaceae,

Calophy/lum, Engelhardia, the Meliaceae, the Myrtaceae, Podocarpus, the

Rhlzophoraceae and Sonneratiaceae, the Tiliaceae and Avicenma. Among the her­

baceous plants. the Asteraceae. Cyperaceae and Poaceae; among the ferns. Pteris

and Stenochlaena palustris.

Several of these taxa percentages vary. For instance. Casuarina, Podocarpus and

the Rhizophoraceae are mainly represented at the bottom and at the top of the

sequence: as for the Poaceae. they benefil at the top trom a decrease in the number of

Cyperaceae. and Stenochlaena palustris disappears when reaching the highest layers.

Many plants are found in a more sporadic way or are more isolated, Iike "ex,Dacrydium, Elaeocarpus, Ficus, Myrica, Pterospermum, Symplocos, the L1lmaceae, the

Mimosaceae and many grasses.

The recalculated diagram (Fig. 26), which excepts the most important mangrove

elements, displays curve shapes that are somewha.t different from the basic ones.

especially near the Rhizophoraceae peaks of il.

S3~OdS

d'1M

"0& ,--,

d'1

36

Il 1 1

= co'" ,...,4""" OO"'CDXr-") r-'l t"""'l '" C"'.I 4.---(,1')

-..~ l"""'t ~-O.::::1000000 r-- l.O..r~-CO\O-r("'.lOa)I.OU'""o

x;.-- - --- CTI O'\O'\O'\CTla:>a)':X)COCO"""'''''''''''''''

S3sn318~S S311!)lJ~ U!l3W01!)NOJ S3n318 S311'J!I'I

'W 01

FIG. 24 SOKO, AP/NAP DIAGRAM

Jf3JVOd

• U . 1 • 1 . • • . • • • 1 . . 1

1 . • 1 • 1 1 • • • 1 • • U • . . •• •

_-.>......1 • 1••U'--_LlLludJ'-- --.........-.._-...........--.......-...-

VMllIVnSVJ

. lIO IlVMlIO:J

3aIMnH 13110~

3V3)V1I3d.lJ

39VJ311VM 3a S311DdS

3Sn3~VJ311VM NOIIVMlIO:J 1 1. M • • • . . . . • 1 • • • . . Il 1

31VlIOllll lIOIIV1393~ 1 • 1 1 • • . 1 1

31\01l91lVM 311311111V 1 1 I.U • • 1 • • 1 1 1 • •• 1 LtJ. 1 LJ

, 0 1 ,...-----,

3M1I91lVM 1

-4 ("'"') OO'CIOXr-l r-l r-J N N CI:---V')

,...., U"'\ ,..., C"I - 0::JO Cl Cl 0 Cl Cl ,...., 1.0 ~ C".I - CIO \0 ~C".fO en \OU""l ~..::-- 0'1 Cf'tCf'tCf'tcnCXl'a:JCXl'CX)m",...,. ...... ,......,.

S3sn318VS S31I~ijV IVij3W01~NOJ S3n318 S31I~ijV

'W Ol

FIG. 25 SOKO. VEGETAL FORMATIONS DIAGRAM

53110clS

'dTII

,. GC ~

'd 'V

38

1

1 1

S3sn318VS S3119HV lVH3W019NOJ

t-"I f"'-.. _ C>

o 000 ,...,. l.O..z <"".l - a::> \,Q ...rC"".lC> co '-OU"')CJ" 0\ en 0"'1 O'l co a;) CD CD a;) ......

'W OT

FIG. 26 SOKO. RECALCULATED API NAP DIAGRAM

'******************p I.A Congress VI. Malang. July'92

Il.Interpretation elements

39

The bulk of the diagram. in which we found microplancton cysts everywhere, is

dominated by the mangrove and back mangrove associations (Fig. 25). Those two

vegetal formations are subject to several changes along the section. but the mangrove

forest is always conspicuous. Its curve is mainlydue to the Rhizophoraceae, which give

three peaks in the KU 94. KU 103 and SAM 34 spectra. This vegetal association took

place not so far from the sampled sites. Such a conclusion is in goOO accordance with

the sedimentological analysis (T. Djubiantono. 1992), which give granofacies of intern

mangrove deposition within the b1ue clays.

The comparison between Figures 24 and 26 shows that the non· mangrove tree

frequency IS still important. This very curve is subject to several changes.

Beyond the shoreline developed a swampy forest and a frankly continental vegeta­

tion where tl-le rain forest elements dominate the more open forest ones (Fig. 25).

Figure 25 also shows that the Cyperaceae get lower in frequency when going from

the bottom to the top of the section, and that the Poaceae follow a reversed tren<j,

Although Figures 24 and 26 give a rather regular picture of the frequencies, the

oscillations we see on Figure 25 for each vegetal association lead us to quality those

general observations.

The tirst zone -spectra KU 73 to KU 96- has higher tree and fem percentages. The

Cyperaceae and the rain forest e1ements are very important. pointing to a humid period.

Between the KU 97 and KU 107 spectra. the AP / NAP ratio decreases, owing to

larger Poaceae frequencies. We observe small oscillations where the grasses (Poaceae,

Cyperaceae) oppose to the rain forest plants. The latter progress in KU 100. KU 103 and

KU 107.

The NAP group drops drasticaJly in the SAM 25 layer. No Poaceae. and only a few

Cyperaceae have been found here. Besides the rain forest pollen. other taxa from the

more open formation get here their maximal values. while Podocarpus imbricatus

disappears. This open vegetation indicates a drier period.

ln samples SAM 27 and SAM 28. we get fewer trees and more Poaceae, with a more

open character of the local vegetation.

Between the SAM 29 and KU 130 spectra. we find again altemances between a rain

forest-like and a more open vegetal formation:

u*********"''''''''**P 1A Congress VI. Malang. July'92 40

- ln SAM 29. when compared wlth the SAM 28 layer. the Cyperaceae and the

Poaceae decrease whlle the raln forest elements progress. especlally wlth Podocarpus.

as the open forest plants and the ferns do

- ln SAM 32 and SAM 33. the Poaceae progress and the trees decrease

- in SAM 34, whlch is one of the spectra where the mangrove association was

the most important. we find a few Poaceae and Cyperaceae: the trees belong to the

raln fores!.

- Between KU 128 and KU 130. we have a new Poaceae and Cyperaceae

Increase. correlated wlth a drop of the tree frequency

Figure 26 shows sharp variations ln the KU 133 spectrum many trees and a few

grasses From this layer to the KU 138 sample. we observe a progressive decrease of

the trees and a progression of the fems. Rain forest taxa become less important. the

open forest and swampy forest elements disappear The NAP group IS domlnated by

the Poaceae. and Casuartna holds steady.

Those observations show a rather open envlronment. disturbed by the volcanlc

actlvlty The sOli IS covered by Poaceae and ferns

III. Paleoecological Conclusion

"The influence of the mangrove forest remains even ail along the studied

section at Soko.

The flrst twenty meters of blue clays (Zone A on Fig. 27) show the dominance of the

raln forest trees. the Cyperaceae and the ferns.

"Ouring this stage, the continent was occupied during this stage by a rain

forest like formation.

The following twenty meters (Zone B) show an opposition between the grasses and

the rain forest e1ements

*Zone B presents an alternance between rain forest and open formation

periods.

From the top of the blue c1ays to the bottom of the conglomeratic layer (Zone C),

we find an increase of seasonal or open forest taxa and then a Poaceae dominance

*This zone includes, at least at its base, a less humid period during which

an open forest developed in the plain and on the hills.

41

KI!

138

VI E....134.,.,

::0... 1])...J-«.,.,V'lI 130.... 129~

128~

0a: SAlI 3e.oC

Hc 29CE....w:0 28~

~

:z210

'-J C2~

KU107105

103 8--102101100

97

9694

E -- 92V'lI 91.... --.::> aa0 ........a> 86 A"".... ae....J

al~

80""...la

7615

73

FIG. 27 SOKO. POLUNIC ZONES

u ..... u •••••••••p 1A Congress VI, Malang, July'92 42

Then we find the deltalc conglomerate. which Ylelds the oldest mammals found on

the site. The upper conglomerate samples. like the lower part of the overlying sandy

clays (Zone D), show again alternatlng raln forest / more open vegetation

·The uppermost pollinic spectra (Zone E) present a locally open vegetation,

probably impoverished by the volcanic activity, where Poaceae and ferns

dominate.

It IS worthy to notice on Figure 25. at the top of the fossll- bearing conglomerate of

Kedung Cumpleng, the relative opposition between back mangrove and swampy ferns

on one slde, and mangrove forest on the other side This could weil correspond to a

smaller oscillation of the sea level (eustatism?) one million years age.

' p I.A Congress VI, Malang, July'92 43

D.PALEOGEOGRAPHICAL SIGNIFICANCE OF THEKALiUTER SERIES

by François 5ÉMAH

1.The informations gathered from the Kaliuter area

Ses/des the dlscovery of new fossll-beanng sites. the study of Kaliuter area gives

new Important data about the geologlcal evolution of this northern part of the Solo

depress10n

1.1.The deposition environment

The whole of the studied sections show that the deposition envlronment cannot be

descnbed as open-sea: recessive conditions appear very eany in the area, as observed

near the basls of the Sarong section. more than 2 m.yrs ago. The layers described by

L J C van Es (' 931) as the Lower Kalibeng G/obigerina mans are ln fact sandy mans

deposlted in a shallow sea. The banked limy facies contains many littoral fossils. and

the blue clays were deposited near a mangrove formation (tidal area).

Ali along the Sarong, Soko and Kedung Krujuk sections. we observe a global

recesslon of the the sea.

1.2.The influence of volcanoes

The Influence of volcanic activity on the sedimentation is very important in the

hOrizontal series (tuffaceous sands. breccia... ). Sut it can be observed also in the folded

marine series'

-Directly, as we noticed the presence of severa! cineritic banks

-Undirectly. by the measurement of magnetic susceptibility. Such measurements

give an idea of the magnetic minerai content of the sediment, which is itself largely

dependent on the volcanic minerais content. The analysis show that the volcanic

influence has been more important in the Soko section than in the Sarong one, and

appeared also eanier (Fig. 28 and 29).

-

44

~~

~~

-- _: 1

~~~è-OJIL'­E-=-~--;-:-'-7-:-i i~

o

r'<

10

FIG. 28 BARONG. MAGNETIC SUSCEPTIBIUTY

45

-,

-- -- -- --- - -- (.)---------.-------.-~~-

- - - - - - - ~ ~ ~ = 1 __

--- - _. ------ - - ---

10o

wll.

1«J-r-,.-~---..... 1(:

«uL-----.---.--~-___r--_r_-~-~

FIG_ 29 SOKO. MAGNETIC SUSCEPTIBIUTY

...****************p 1A. Congress VI. Malang, July'92 46

The fine-grained blue ctays themselves, whlch contaln a lot of smaller magnetlte

cnstals, are likely to be the result of the weathenng of volcanic ashes which thickly cover

the flanks of the volcanoes

1.3.Tectonics

From the structural pOint of view, the Kaliuter area gives two important data:

The first one is the tectonic unconformity between the folded series and the hOrizontal

ones This unconformity represents the last folding phase of the Kendeng hills, and can

be dated at about 0.7 myrs ago (BrunhesjMatuyama boundary).

The second one is the presence of the deltalc fossil-bearing conglomerate at Kedung

Cumpleng. This conglomerate contalns a lot of Iimestone pebbles transported bya river

It proves that. one million years aga, the Kendeng hills di<:! already exist northwards, and

that they had already been colonized by continental mammals and by man.

The question of the age of these emerged reliefs IS still unsolved. But we can assume

that they are somewhat ald. If we go downwards ln the Kaliuter series, the next

unconformlty can be found ln Miocene layers, at the contact between the Kerek and

Lawer Kallbeng formations. We think that the first Kendeng "ridge" formed at those tlmes.

but was not definitely emerged. The emersion was helped by eustatlc drops of sea-Ievel

(slnce 2 4 m yrs ago) and/or bya contlnuous uplift

II.Palaeogeographical implications

On a larger scale. we can present a more concise vision of the geological events

whlch took place ln the Solo depression when Pithecanthropus arrived ln Central Java

For that purpose, we shall use also the available data on several other sites like Sangiran,

Bringinan, Onto-Simo and Gemolong (F Sémah, 1986; S. Sartono et al 1984) (see Fig.

30 and 31).

Il.1.Sea level oscillations

It seems established now that a recessive evolution of the sedimentation took place

ln the area at the very beginning of the Matuyama period. 2.4 m.yrs ago, the older

Kendeng reliefs contributed ta the recession of the sea by forming a barrier northwards.

But further eustatic sea-level oscillations are hardly visible in the stratigraphie

sections. except for the one pointed by pollen analysis near the Kedung Cumpleng

conglomerate (see above).

-AU~rU _ -' 1 MATUYAMA 1 BRUNHES

J>

J>

J>

::

Ci<

::;-1

'-,Fl

=- :>- 1-~

==J>

.:'- -

)

)

oUl1

-'-(',

-,r, e:!T ~

-.

[1-= :JO ï:" =.;edJrI€ ~,-.:~. ,,- -= ~

isolees~lJi.;

)

(

o1

<---r,

1-,

-(~:

~ Loi::: ,

J -, ,.JO'

1

Pu:onQ(.;(

','

:',

OLDUVAI JARAMILLO_____1 ~ .~ _

n..,lJl1

r- CJ'~rlc.ll,:,r, CiE =- volconsCi 0 n=,I : Ci e Dr e 5 5 10(,

1

r, ,:d Il) E- (, ';. 5 u:::

PI~ '= ChE:::

:=:Cd) -= S 'v'DI,:

~(---E ["'"1 ET'; 10 r ""1 ------~)

(

(

~-:: -~

-r

-:: ,--:- ~

-:: :::,,r, (T

1: 1 \ 1.1111

, III

l ' " 1

-=., \

'-- -,"" -

t 'll+ l' ',i

Il \! l '1 \ 1111 +

! 1 1 l : 1 1 li i 1 ~ ! '

Illl' l'II! \1\1

3:-0nfTl::: rl'["Tl Ln

1

----~)~----------------~ t-(-------=o?c .. :r .-: .- - _

::!'G>woG>moroG>f)»rm<mZ-l(J)

Z-lIm(J)

oroClm"'t):IIm(J)

~oz

111111111 :111": 111\11 ;1111 1 \llllll' ; 1 Il1111"1111111 '11111: III Il! 111: l 'l, l'

.= 1-

=-

:::. 0('9l 0[", i. LlJf'lDlenc.

Lv •

48

.......

•••0.6m.a.

.• :

- ,-.-

--,..-.- ,..-.-

.--- ----- ---- ,...,.-- -- .-- --- r- ------ - ,..- ,......, --r- - .....- ---

-,,--

,,-...J ... --~- ___.--- _........---

--•_c~--_~

""1~.- ._ "l -

[:':::::'.:':-1 dépôts.:.;......; volcano-sédimentaires

fIg collines de Kendeng

_ dômes (couchesptio-p1éistocènes)

b~.~.1 conglomérat K. Cumpleng

~ marais littoral~ (argiles noires)

~ lagune. mangrove~ (argiles bleues)

r:::-::I mer~ (sédimentation calcaire)

10 km

FIG. 31 PALEOGEOGRAPHICAL EVOLUTION

.-

~ faciès de fermeture de la lagune

*** ......*****....p 1A. Congress VI. Malang, July'92

11.2.The larger volcanoes

49

We know that the larger volcanoes in the Solo depression became active at ca. 2

m yrs ago (see Y. Bandet et al., 1989; R.C. Mauryetal., 1987). The oIderworks by Dutch

geologists (see for instance A. W. van Bemmelen. 1949) said that the Gunung Wilis

alone, far to the East. was active at those times. Some of its products could have been

transported westward to Sangiran.

ln fact, the Sangiran lahars. datJng back to the Plio-Pleistocene boundary, are

sometimes very thick. They more likely originate from a doser volcanic centre, like the

Lawu volcano. These lahars contributed to pond up the Solo lagoon, and gave more

continental conditions in the Sangiran area (the Pucangan swampy clays).

These larger volcanoes played a large part in the recession of the sea:

·Directly, by the ponding up of the lagoon with eruption products.

·But also by the simple sedimentation of weathering products of volcanlc effluents.

The thick clayey Upper Kalibeng and Pucangan unrts originate from the weathenng

of volcanlc ashes and of the volcanic cones.

Along the Kaliuter sections. we observed an abrupt change above the so-called

banked limestone facies. We can expiain this sedimentation rupture as a change in the

source of the sediment:

·In the lower part of the sections. sedimentation was linked with a limy source, that

is the Kendeng hills to the North.

·In the upper part. the origin of the sediment changed and it comes from a Southern

volcanic province.

This change progressed gradually northwards. At Gemolong. the b1ue c1ays appear

ca. 2.4 m.yrs ago. At Soko, at the end of the OldlNai event, ca. 1.7 m.yrs ago. At Barong.

several kilometers to the North. weil after the end of the OldlNai event. We see that the

horizontal changes of facies are very rapid and important in the Solo depression.

Therefore, our stratigraphicaJ approach has to consider geooynamically the geological

events which took place at those times; it cannot be restricted to an usual

lithostratigraphic definition of geological formations.

For instance. the c1ayey swampy deposits called "Pucangan" at Sangiran are

synchronous with the b1ue c1ays deposits at Kaliuter. The facies depends on the

palaeogeographical conditions: c1ays deposited under the form of black clay at San­

giran, and of b1ue clay at Kaliuter (nearer to the sea). Lithostratigraphical correlations

between "Pucangan" and "Upper Kalibeng" facies between the two areas IS therefore a

nonsense from the chronological point of view.

"****UH'*****"**"P 1A Congress VI Malang, July'92

11.3.The Kendeng hills

50

Several researchers during the Dutch penod thought that a folding phase occured

near the Plio-Pleistocene boundary (ie. near the Sangiran lahars now dated at 1 7 m yrs

ago) Our observations do not confirm this view. The transition from the lagoonal facies

to more swampy conditions at Sang/ran was mainly linked to the volcanic activity.

The last fOldtng phase of the Kendeng hills we recognlzed dates back to the

Brunhes/Matuyama boundary. It marks the definitive disappearance of marine Influence

ln the Solo depression, At Sangiran and Onto-Simo. we observe a clear change in the

sedimentation, wlth the deposition of the Grenzbank, a conglomeratlc bed which mixes

manne and continental elements. At Kaliuter, we find the so-called transltional beds (with

beach deposlts) descnbed above.

The Grenzbank and the disappearance of manne influence at Sanglran 15 therefore

the Indirect trace. In the depression. of this last folding phase of the Kendeng hilis

Then we f1nd the volcano-sedimentary Kabuh deposlts ail over the area VolcanlC

actlvlty became more and more intense ln thearea (Notopuro breccla), and the Kendeng

hills were eroded, glvlng the geologlcallandscape its present aspect

BIBLIOGRAPHY

BANDET, V., F. SÉMAH, S. SARTONO, et T. DJUBIANTONO, 1989.

Premier peuplement par les mammifères d'une région de Java Est, à la fin du

Pliocène âge de la faune du Gunung Butak. près de Kedungbrubus (Indonésie).

C.R Aead. Sei. Pans, 308, Série Il, p.867-870.

BEMMELEN, R.W. van., 1949,

The Geology of Indonesia and adjacent archipelagoes.

Martlnus Nijhott ed., Den Haag, 3 vol., 732 + 265 pp.

.........................p 1A Congress VI. Malang, July'92

DJUBIANTONO, T., 1992

51

Les derniers dépôts marins de la dépression de Solo, Java Central, IndonésIe

Chronostratlgraphie et Paléogéographie.

MémoIres Semenanlung, 1., 206 pp

ES, LJ.C. van., 1931.

The age of Pithecanthropus.

Martlnus Nijhoff ed., Den Haag, 142 pp.

KOENIGSWALD, G.H.R. von, 1940

Neue Pithecanthropus-Funde 1936-1938

Dienst v d. Mljnbouw Ned./ndlé, Wetensch.Med., 28, 236 pp.

MAURY, R.C., R. SOERIA-ATMADJA, H. BELLON, J-L. JORON, Y.S. YUWONO

et E. SUPARKA, 1987.

Nouvelles données géologiques et chronologiques sur les deux associations mag­

matiques du volcan MUria (Java, Indonésie).

CR. Acad.Sc. Pans, t 304, Série Il, 4, p.175-180.

SARTONO.,S, SÉMAH, F. ET T.DJUBIANTONO, 1984.

Paleomagnetic results from the Bringinan and Gemolong Domes (Central Jawa).

Correlation with the Sanglran Section.

Bu/etin Ge%gi, Jurusan Ge%gi, ITB, 13, p.17-21.

SÉMAH, A.-M., 1986.

Le milieu nature/lors du premier peuplement de Java.

Résultats de l'analyse pollinique.

Thèse de Doctorat ès Sciences Naturelles, Université de Provence, 3 vol.,

188+ 119pp.

••••••••••••••••••p 1 A Congress VI. Malang, July'92

SÉMAH, F , 1986.

Le Peuplement ancien de Java Ebauche d'un cadre Chronologique.

L'AnthropologIe, 90, n' 3 ,p. 359-400

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