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PROCEEDINGS mDO NESIAN PETROLEUM ASSOCIATION

Sixteenth Annual Convention, October 1987

AN OVERVIEWOF SOURCE ROCKS AND

OILS

IN INDONESIA

Kevin

M.

Robinson *

ABSTRACT

Source rocks in the hydrocarbon productive basins in

Indonesia can be classified as lacustrine, fluvio-deltaic and

marine. Lacustrine source rocks are the most productive,

and have sourced most of the oil in Central Sumatra,

some of the oil in the Sunda Basin and also possibly oil in

the West N atuna Basin. Fluvial-deltaic source rocks are

the most common and widely dispersed and have sourced

oil in the majority of foreland (back-arc) basins of Western

Indonesia. Marine source rocks probably occur in Eastern

Indonesia, bu t are poorly documented. However, they may

have sourced oil in the Salaw ati Basin and eastern Sulawesi.

Positively identified producing source rocks are all Tertiary

in age, although PrsTertiary (Permian/Jurassic) rocks are

suspected to source oil in the Bintuni and Bula (Seram)

Basins and are also a possible source in eastern Sulawesi

and t he Banggai-Sula area east of Sulawesi.

Crude oils in Indonesia can also

I

be characterized as

lacustrine, fluvio-deltaic and marine based on a range of

geochemical p arameters, including pyrolysis-gas chrom ato-

graphy on the oils asphaltene fraction and GC-MS bioma rker

data. Lacustrine oils sourced from non-marine algae are

generally low-medium gravity, waxy, low sulfur oils and

often contain'unusually high concentrations of C3O 4-methyl

steranes. Marine oils derived from marine algae are low-

medium gravity, low w ax, medium-high sulfur oils and con-

tain C27-C29 diasteranes and steran es in relatively high

concentrations compared to other oil types. Fluvio-deltaic

oils

derived from higher plant, terrestrial organic matter are

medium-high gravity, waxy, low sulfur oils. They contain

abundant higher plant resin derived C30 alkanes and low

obviously dependent on the original o

source rock.

The main objectives of this paper are

1)

Categorise the source rocks of the

producing basins of Indonesia int o

ine algal), fluvio-deltaic (terrestrial)

ine algal).

2) Describe the general geochemical ch

different source rock types.

3) Develop a scheme to classify Indone

rine, fluvio-deltaic and marine bas

chemical analyses.

SCOPE

This paper a ttemp ts to cover all the

producing basins of Indonesia (Fig.

1

source rocks within the basins is prima

ously published data and

on

experience

However, source rocks within some

unknown, postulated or unconfirmed by

rock correlation studies. The oil classif

detailed geochemical data

on

one .hu

samples covering all the major hydr

basins of Indones ia (Fig. 1).

SOURCE ROCKS

The major source rocks or suspec

the hydrocarbon productive basins in I

in Table

1

and discussed below by de

ment.

© IPA, 2006 - 16th Annual Convention Proceedings, 1987Disc Contents

Contents

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9

where in Indonesia, particularly in the foreland (back-arc)

basins of Western Indonesia, where rifting occurred in the

Early Tertiary behind a volcanic island arc system.

The deep lacustrine shales of Central Sumatra were de-

posited in subsiding basins, under tropical climatic condit-

ions. The lake had no annual turnover, resulting in anoxic

bottom waters, which favoured preservation of organic mat-

ter rich in non-marine algae (Fig. 3;Williams e tal , 1985).

In shallow rift basins, where subsidence was only equal to

the rate of deposition, humic rich lacustrine shales and

coals wiU have formed instead (Central Sumatra Coal zone,

Table

1).

Deep lacustrine shales are some

of

the most oils'product-

ive source rocks in the world. In Central Sumatra they ac-

coun t f or over half of Indonesia's o il reserves (Woodside,

1984). Immature, lacustrine shales typically contain be-

tween 1.0 to 10.0 total organic carbon and

50

to 100

oil prone, fluorescent non-marine algal derived amorphous

kerogen. The pyrofysis yield (Sl+S2) s variable ranging

from 4.0 to 75.0 mg hydrocarbons/gm rock, but is often

very high. Hydrogen indicies are typically in the 400 o

900 range, wit h elem ental kerogen hydrogen/carbon rat-

ios usually greater tha n 1.4 (Table 2). Specific non mar-

ine algae such as Botrycoccus braunii or the non-marine

planktonic algae

Pediastium

spp can sometimes be ident-

ified in the samples, while inp ut from Botryococcus and

dinoflagellates, can be inferred from GC-MS biomarker

data (Wolf et aL 1986; Brassel et al., 1986,Seifert and

Moldowan, 1980).

Fluvio-DeltaicSource Rocks

Fluvio-deltaic source rocks containing terrestrial

de-

rived kerogen are the m ajor source rocks of m edium gra vity,

waxy crude

oils

in many of the foreland basins of Indo-

nesia. In South Sumatra and N.W. Java (Sunda, Ardjuna,

Jatibarang) Basin, Oligocene Talang Akar coals and shales

have been identified as a major source of the oil, while in

the Malacca Straits of Central Sumatra, Sihapas coals have

generated some of the oil (Table 1 .

In the East Java sea, Oligocene Kudjung I11 coals and

shales and in the Barito Basin, Eocene Tanjung coals and

shales are speculated to be the source of the oil (Tabb

1).

Although neither of these co rrelations are proved in the

well documented geochemically (Com

1978; Durand and Oudin, 1979; Hof

Oudin and Picard,

1982;

Schoell

et

a

aL 1985). The major source rocks be

Miocene Balikpapan Group. It represen

progradation which has continued,

interruptions, through to the present d

card,

1982).

The sediments were depos

flowing river system into a subsid

north-south axis. A full suite of facie

sedimentation were deposited (Fig. 4).

tent is relatively high throughout the

(often

>2. ),

but the best source

delta plain where coals tend to be

5, Thompson,

1985).

Generation of hydrocarbons within

largely controlled by maturity, as thick

rich source rocks are present throughou

basin. The top of the oil window in th

depending on temperature gradient, b

about 2800 - 3000 meters (Schoell e

and Picard

1

982) have demonstrated

may also be important in the hydroc

and type (oil or gas) within the Kutei B

the

oil

window is completely within the

generated oil cannot be expelled and i

s i tu gas. The Kutei Basin hydrocarbon

may also be applicable in the Tarakan

men tation occurred along similar lines.

Fluvio-deltaic coal and shale source r

large volumes of oil in Indonesia and ac

production of hydrocarbons in the A

Basins. Fluvio-de ltaic shale source rock

2.0-10.0 tota l organic carbon with

6.0 to 20.0 mg hydro carbons/gm rock

tain 40.0 o

80.0

total organic carbon

rolysis yields of 150-300 g hydroca

ble 2).

Fluvio-deltaic coals and shales gen

higher plant terrestrially derived organi

predominantly of vitrinite with seco

cutinite and resinite. The total amount

exinitic kerogen is usually in the 10-3



rocks usually have high pristane/phytane. ratios e 3 . 0 ) due

to deposition in an oxik environment. They

also

have relat-

ively high co ncen trations of waxy n-paraffins and

C30

cyclic alkanes (identifiable b y GC-MS) derived from higher

plants.

Marine Source R ocks

Marine algal rich source rocks are the m ajor source of oil

in the world. But in Indonesia none have been positively

identified in the literature. However, based on crude

oil

characterization a marine carbonate or calcareous shale

source is suspected in the Sala wati Basin of Irian Jaya (Pho a

and Samuel, 198 6; Hughes, 198 4) and in eastern Sulawesi

(Table

1).

Deposition of the source rock would have

occurred under anoxic conditions in a restricted marine

basin. In Salawati a likely source is Early Miocene Klamo-

gun

carbonates and shales (Fig. 6), while in eastern Sula-

wesi Early Miocene shales and carbonates are a possible

source or alternatively Jurassic m arine shales and carb-

onates.

Immature, marine source rocks capable

of

generating

oils in the Salawati Basin and Sulawesi area would typical-

ly be expected to contain 0.5 to 5.0 TOC, moderate to

high

pyrolysis yie lds (2.0-30.0 mg hydrocarbon s/gm rock)

and an orga nic facies comprised mainly of oil prone , mar-

ine, algal derived amorpho us kerogen. Pyrolysis hydrogen

indicies should be

in

the 300-600 range and kerogen ele-

mental hydrogenlcarbon ratios

>

1.2 (Table 2).

Re-T ertiav Source Rocks

All the Indonesian source rocks positively identified

and correlated t o oil accumulations in the published liter-

ature are T ertiaty in age. However, pote ntia l Pre-Tertiary

source rocks have been identified

in

Eastern Indonesia

(Chevallier and Bordenave, 1986) and are related to pre-

break up

of

the Australian Plate

in

the Mid-Jurassic (Peck

and Soulhol, 1986). In the Bintuni Basin

of

Irian Jaya

two PrsTertiary sourced

oil

types possibly exist (Chev-

allier and Bordenave, 1986) The major source of most

of these oils is thought to be Late to Early Permian Aifat

shales with Jurassic Tipuma shales or possibly U pper Permian

Ainim coals acting as a source for the other

oil

type

(Wiriagar oiI).All of the source rocks in theBintu ni Basin are

suspected to contain a predominantly terrestrial organic

ses such as API Gravity, Weight Sulphu

ography, plus, more detailed analyses s

topes, Pyrolysis-GC

on

the oils asphalte

Chromatography-Mass Spectrometry (G

analysis on the saturate fraction of the

o

ics listed are

for oils

generated at norm

levels (Ro 0.5 - 1.0 ) and unaltered

as thermal o r biological degradation o r w

Bulk Data

Bulk Data such as API gravity, we

gasoline range analysis and whole oil/s

chromatography give useful indicators

of an oil, but are not detailed enough

ify its gen etic origin.

Algal sourced oils, marine or no

have low-medium API gravities (20-35O)

tane ratios less than 3.0. Initial differ

marine algal oil from a marine algal

oil

based on sulphur conten t and wax c

oils are typically high wax (C31/C19

(< 0.2 wt ); while marine oils are low

C19), high sulphur >

0.2

wt ). Flu

oils usually are medium -high API grav

sulphur high wax crude

oils

(Table 3). T

have high pristanelphytane ratios 3.0

of the source rock in a n oxic enviro

McKirdy, 1975).

The

n-alkane distribution

of

oils (F

useful in distinguishing different

oil

is far from definitive. Lacustrine

oils

t

modal to broad n-alkane distribution d

C19 and C23-C33 n-alkanes from

(Gelpi eta l,1 97 0; Mol dom eta l., 1985)

tanelnC17 ratios. Marine

oils

usually

concentration of higher molecular wei

wax content) and Pristane/nC17 ratios

taic (terrestrial) oils usually show a broad

ion or a predominance

of

waxy (C2

Pristane/nC17 ratios

> 1.0.

Carbon Isotopes

Carbon isotopes

on

whole

oil,

satu

other fractions of the crude

oil

have

entiate marine oils

from terrestrial

oil



100

and to some extent experimental technique. The idea

behind the analysis, is th at asphaltene molecules are small

kerogen molecules and representative of the original kero-

gen in the source rock (Pelet

e t

aL, 1986). Pyrolysis-GC of

the asphaltenes can then be used to identify the original

kerogen type of the oil’s source rock, based on the general

distribution of hydrocarbons on the pyrogram. This can

then be used to characterize the

oils

into different oil

types (Fig.

8).

Also the relative n-octene, m+p xylene and

phenol content of the oil’s asphaltenes can be quantified

and plotted on a Ternary diagram. (Fig. 9, modified after

Larter, 1985) to determine oil type and the kerogen type

of the source rock. Th e pyrolysis-GC on the oil’s asphal-

te ni s is performed at 550OC.

A

typical lacustrine

oil

pyrogram (Fig. 8) shows well

developed alkenes/alkanes doublets from C5-C35,with part-

icularly high concentra tions of C15-C30 n-alkenes/n-al-

kenes derived from non-marine algae. Characteristicly

aromatics and phenolic compounds are virtually absent

from the pyrogram.

A

typical marine

oil

asphaltene frac-

tion pyrogram shows a decreasing concentration of

n-al-

keneln-alkane doublets with higher molecular weight and

moderate concentrations of aromatics and phenols.

A

flu-

vio-deltatic oil shows a broad n-alkene/n-alkane distribution

and contains the highest concentration of aromatics and

phenols out of all the

oils.

Prist-l-ene also tends t o be high

in

fluvio-deltaic

oils.

A

plot of the

oil’s

n-octene, m+p xylene and phenol

content (Fig. 9) can clearly distinguish lacustrine oils from

fluvio-deltaic oils. But marine oils, probably due to lack of

data, cannot be distinguished from lacustrine oils. Oils pre-

sumed to be from lacustrine sources in the West Natuna

Basin and some of the oils

in

the Sunda Basin plot away

from the deep lacustrine oils of Central Sumatra. This may

be due to deposition of the

oils’

source rock in a different

lacustrine depositonal environment than that proposed

for Central Sumatra. Possibly it was shallower and/or more

saline?

GC-MS

Biornurker Data

Lacustrine, marine and fluvio-deltaic

oils

in Indonesia

can be distinguished based on Triterpane (m/z 191) and

Sterane content (m/z 217). Other biomarkers can also be

used such as Bicyclics (m/z 123), Isoprenoids (m/z 183),

oils in

Indonesia te nd to have simple

ions containing only pentacyclic 17dh

C35 plus moretanes and little else. The

is maturity and organic facies influen

than 1.5 and Tricyclic Terpanes (not sh

centrations or absent.

Marine

oils

also have relatively sim

retane distributions, but

in

Indonesia

concentrations of C3

1

-C35 hopanes..

to deposition of the source rock in an

environment, with high bacterial acti

tend to range from 3.0 to 1.0. In Ind

is often in relatively high concentratio

derived oils (Phoa and Samuel, 1986).

be due to transportation of resistant

into the marine basin and not indicat

source for the

oil.

Noticeable other

compounds, commonly found in ass

oleanane, are absent or in very low con

oils also tend to have relatively high

tricyclic terpanes.

Fluvio-deltaic oils have very character

tributions with high concentrations of

resin derived cyclic alkanes and the C

oleanane.

This

is in addition t o th e norm

and m oretanes. The C30 derived comp

eristic peaks on the m/z 19 1, 163, 17

mass ion scans (Fig. 11). Tm /Ts ratios

rived lndonesian oils tend to be relati

from 6.0 to

1

O

Steranes mfz 21

7

Steranes relative to hopanes tend to

trations in non-marine oils, whether th

fluvial-deltaic in origin (Table 3). Ty

hopane ratios are <0.2 in non-marin

marine

oils

(Moldowan

etal.,

1985). D

centration of steranes, it can be diffi

sterane (m/z 217) scans in non-marine

column of the GC-MS is overloaded .

Deep lacustrine

oils

usually contain

C27-C29 steranes and diasteranes (Fi

low c oncentrations, and usually have a

centration of C27 and C29 steranes (



oils around the world. The Salawati Basin oils show similar

Triterpane and Sterane distributions to oils in the Mara-

caibo Basin of Venezuela (Fig. 14). These oils are sourced

from the Cretaceous La Luna Formation which is an or-

ganic rich carbonate (Talukdar etal., 1986). This would

suggest a similar type of source rock may have generated

at least so me, of the Salaw ati Basin

oils

(klamogun carb-

onates and shale?).

Fluvio-deltaic oils have a very characteristic m/z 217

Scan usually containing only C29 steranes and diasteranes

(Fig. 12). The dominant compounds on the scan are C30

resin derived cyclic alkanes, which are also present on the

m/z 191 triterpane scan. A comparison of triterpane and

sterane distributions (Figs. 1 5 and 16) of fluvio-deltaic

oils from South Sumatra, Kutei and Tarakan Basins shows

little variation between them, suggesting the organic facies

and original higher plant input is similar in all these basins.

A plot of C27-C29 sterane composition (Fig. 17) can dif-

ferentiate lacustrine/marine oils from fluvio-deltaic oils,

but cannot seperate lacustrine and marine oils from each

other.

CONCLUSIONS

1) The sou rce rocks of Indonesia can broadly be classi-

fied into lacustrine (non-marine algal), marine (marine

algal)

and fluvio-deltaic (terrestrial). Althou gh signifi-

cantly more oil/source rock correlation work needs to

be done or published to confirm the source rocks of

many Indonesian oils.

2) The identified source rocks are of Tertiary age, although

Pre-Tertiary source rocks are probably generating oil

in some parts of Eastern Icdonesia.

3)

Crude oils can be characterized as lacustrine, marine

or

fluvio-deltaic sourced oils based on a combination of

geochemical data. This includes standard bulk data,

Carbon Isotopes, Pyrolysis-GC of Asphaltenes and GC-

MS biomarker analysis. Lacustrine oils need further

work to subdivide deep, fresh water lacustrine oils from

shallow lsaline lacustrine oils.

4) Suspected Pre-Tertiary sourced oils should be analysed

and classified to see what type of

oils

they are and if

they show any differences, (particularly in biomarker

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TABLE 1

SOURCE ROCKS OF

INDONESIA

HYDROCARBON BASIN* MAJOR SOURCE AGE DEPOSITIONAL ORGANIC GENERAL SO

PRODUCTIVE

TYPE

ENVIRONMENT FACIES OIL TYPE REF

BASINS OF

SOURCE ROCK

North Sumatra Foreland

Foreland

Foreland

Foreland

Foreland

Foreland

Foreland

Cratonic

Foreland

Foreland

Foreland

Inner Arc

Inner Arc

Baong shales? M-L.Miccene

Bampo? )

) - Oligocene-

Bruksah?? ) E.Miocene

Marine

Marine

Marine

Deltaic

Marine algal/

Terrestrial.

Marine

algal/

Terrestrial

Terrestrial/Non

marine algal

Non-marinealgal

Gas/Lght

01

Situ

198

Soe

Kin

Central Sumatra

Pematang Eocene-

Brown shale Oligocene

(major)

Coal zone

(minor)

Sihapas

coal E.Miocene

and coal shale

Pematang brown

Eocene-

shale? Oligocene

Talang

Akar

Late

Oligo-

coals/coaly cene-Early

shales Miocene

Deep Lacustrine G M . Gravity, Will

waxy, L.

198

Sulphur

Condensatel

light oil

M.

Gravity, Ma

zie

sulphur

L-M. Gravity, Lee

waxy, L.sulphur

M-H Gravity

oil,

L-Mod.

waxy, L. sulphur/

condensate

M.

Gravity

M

waxy, L. ,ulphur

Bus

198

M.

Gravity, Gor

waxy, low Wah

sulphur

198

M. Gravity, Soe

mod waxy, low Rus

sulphur Bish

M-H Gravity,

low-mod waxy,

low sulphur

M.

Gravity, Sie

waxy, low sulphur

M.

Gravity, Dun

waxy, low

197

su lph ur Tho

198

M.

Gravity, Sam

waxy, low

sulphur

Poll

Shallow lacus-

trine/marsh-bog

Fluviodeltaic

Terrestrial

Terrestrial

entral Sumatra

(Malacca Straits)

Deep lacustrine

Fluviodeltaic

Non-marlnc algal

Terrestrial

outh Sumatra

N.W. Java

(Sunda)

N.W. Java

(Ardjuna

Jatibarang)

E. Java Sea

Banuwati shales

Early Oli-

Talang

Akar

Oligocene

coals/shales -E. Miocene

TalangAkar Oligocene-

coals/coal y E. Miocene

shales

Kudjung Oligocene

Unit 111 shales

and coals?

Barat shales? Late Oligo-

gocene

cene

Deep lacustrhc

Fluvio-Deltaic

Non marlne algal

Terrestrial

FluvIo-Deltaic

Terrestrial

Fluviatile Terrestrial

West Natuna

Barito

Kutei

Non-marine algal/

bacterial/terres-

trial

Terrestrial

Lacustrine

Tanjung coals?/ Eocene

shales?

Balikpapan Middle

coals and Miocene and

shales and Younger

Younger Deltaics

Latin coals and

M.

Miocene

shales?

Tarakan and Bu- Pliocene

nyu

coals and

shales?

Fluvio-Deltaic

Deltaic Terrestrial

Deltaic

Terrestrial

L-M. Gravity

Low wax, mod-

high sulphur

E. Sulawesi

(Banggai/Sula)

E. Miocene

shales and car-

nonates?

Jurassic shales

and carbonates?

Manusela

carbonateslcalc

Early Miocene Marine Marine

algal

Jurassic Marine

Marine

Marine algal

Marine Akgal?

ula (Seram)

Early Jurassic

Low-M. Gravity O S

low wax, mod-

198



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4

<

4

>

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L

w

A

<

L

w

A

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s

=

P

s

a

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=

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a

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=

S

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c

v

a

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=

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n

h

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=

C

1

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n

h

c

=

2

5

6

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+

2

2

6

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-

1

6



106

a m

o m

~a

w

a -

a

z

m

a

a

Y 0

2

0

a J

W

w w



C E N T R A L S U M A T R A

L A C U S T R I N E SO U RC E R OC K D E P O S I T E D

IN

HALF

G R A B E N

RIFT

B A S I N

.

..

. -

EN

ECHELON

, G R A B E N S

B A L A M A ND R A NG A U B A S I N S

C E N T R A L S U M A T R A

+ +

f t

+

+ +

t

+

+

+ c

+ +



W

”

M



110

I

I

l l 7OE \ 118OE

+

.s

0 a5 6 0 K m

H A N D I L

F IELD

- ssw



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6



112

z

0

0

n

n

c

z m



P Y R O L Y S I S

-

G C O F C R U D E OIL A S P H A L T E N E S

n

L A C U S T R I N E OIL

TYPE I KEROGEN

M A R I N E O I L

T Y P E 11 KEROGEN

I 0 n

C

10 ALK ENE

T TOLUENE

X

= m t p XYLENE

Pf

PR lST

-

I

-

EN

P H E N O L S A L K Y L B E N Z E N E S

T 8 X

I \

F L U V I O - D E L T A IC O I L

TYPE 1II KEROGEN



114

P Y R O L Y S I S - G C C L A S S I F I C A T IO N O F C R U D E OIL A S P H A

USING D I S T R I B U T I O N

O F

N - O C T E N E m

+ p

XYLENE

PHENOL

T Y P E = K E RO

*.

M A R I N E O I L S

( S A L A W A T 1 , S U

N O C T E N E

100 Y o

D e e p

L a c u s t i n e

O i l s

S u n d a B a s i n 1

S h a l l o w

L a c u s t i n e O i l s

( W . N a t u n a / S u n d a B a s in )

F l u v i o - D e l t a i c Oils

[ N W.

Java

,East Java,

K u t e i , T a r ak a n ,

T Y P E 111



L L -

0

w w k

It

t ti

o a

a >

j i -



6

F L U V l O

-

D E L T A I C O I L S

-

I D E N T I F I C A T I O N O F R E S I N

C 3 0 C Y C L I C A L K A N E S

R

B

C 2 9

2 9

30

M / Z 191

TRITER PANE S

R C 3 0 C Y C L I C A L K A N E S

OL = l a d O L E A N A N E

C 3 0 = H OP A N E S

T s ,T m = C 2 7 H O P A N E S

M / Z

217

STERANES

2 9 -

S T E R A N E S

M / Z 163

M / Z

412

D E R



L

A

R

N

O

I

L

T

K

N

2

1

7

.

0

0

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C

2

9

M

/

C

B

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M

l

I

_

.

.

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B

4

4

4

4

4

4

4

4

5

M

A

N

O

IL

T

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2

7

2

2

9

3

3

3

3

3

3

3

C

O

I

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A

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2

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C

2

7

R

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2

9

M

/

C

3

0

M

-

4

M

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3

R

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1

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r

2

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1



118

LACUSTRINE

OIL

*IDENTIFICATION O F

C

30 4-METHY

L

S T E R A N E S F R O M

M / Z

217,231 AND

414

I O N S

ION 217.00

METHYL

ERANES

O N

414 .00

I l l

4oJ

30-



m

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a

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v -

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-

r n d

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0

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9

3

0

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/

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-

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L

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G

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2

9

=

H

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P

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T

m

/

T

:

2

H

P

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3

0

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I

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L

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A

L

A

N

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:

O

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A

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2

4

-

4

C

2

4

T

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A

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1

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S

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l

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3

F

G

U

1



C OM PA RIS ON O F S T E R A N E S ( M / Z 217) IN S O UT H S U MA T RA , T A R A K

A N D KUTEI B A S I N F L U V I O - D E L T A I C S O U R C E D O I L S

R

M / Z

217

T A R A K A N B A S I N O I L

L E G E N D

C 2 9 S T E R A N E S

C

2 9

I

D I A S T E R A

R

C 3 0 R E S I

C Y CL I C A L

bl/Z

217

R

P

R

c 2 9

ljh

R

S O U T H S U M A T R A O I L

bl/Z

217

R

K U T E I B A S I N O I L

c 2 9



C

2

R

S

T

E

R

A

N

E

C

O

M

P

O

S

T

O

N

O

N

N

A

C

O

I

L

T

Y

P

E

S

(

A

H

a

M

e

n

e

1

L

n

M

a

n

o

s

l

u

o

D

a

c

o

s

C

2

g

5

d

2

0

R

F

G

U

1

Translate-1 Overview of Source Rocks and Oils in Indonesia (Robinson

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Transcript of Translate-1 Overview of Source Rocks and Oils in Indonesia (Robinson