© IPA, 2006 - 11th Annual Convention Proceedings, 1982
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PROCEEDINGS INDONESIAN PETROLEUM ASSOCIATION Eleventh Annual Convention, June 1982 Search
CENOZOIC STRATIGRAPHICNOMENCLATURE IN EAST KUTAI BASIN, KALIMANTAN by Edward Marks*,Sujatmiko**,Lki Samuel***, H.'Dhanutirto*,T. Ismoyowati* and BB. Sidik*
ABSTKACT
INTRODUCTION
The Cenozoic sediments of the eastern Kutai Basin, East Kalimantan, are composed of several deposystems that can be distinguished by their lithic successions and separated by disconformities evident on seismic records. Five deposystcms are separated into the following Groups with their subdivisions: the Pleistocene to Recent Mahakam Group, divided into the deltaic Handil Dua Formation to the west and the marine Attaka Formation to the east; the middle Miocene to Pliocene Kampong Baru Grocp, consisting of the deltaic Tanjung Batu Formation to the west and the marine Sepinggan Formation to the east; the middle Miocene Balikpapan Group, containing the upperrnost carbonate to marine clastic Klandasan Tongue of the marine Gelingseh Formation and the paralicdeltaic beds of the Mentawir Formation; the early to middle Miocene Bebulu Group divided into a carbonate Maruat Formation and a deeper water clastic and carbonate Pulau Balang Formation, and the late Oligocene to early Miocene Pamaluan Formation. These Groups and their subdivisions are described at their type and reference localities, and their inter-relationships and boundaries are discussed with vertical and horizontal sections.
* Union Oil C o . of Indonesia -Balikpapan ** Total Indonesie Balikpapan *** 'Pertamiia Unit EP IV - Balkpapan
-
Present multicompany intensive exploration in t k Kutai Basin, as in other parts of lndonesia, has made it imperative that we review and refine previous lithostratigraphic terms in the light of modern concepts. Aims The aims of this work are to get satisfactory answers on nomenclature, which should be based upon the nature of the rock bodies in time and space. In turn, the nomenclature should have value the better to understand the distribution of potential and realized reservoirs found in the Kutai Basin. Problems Previously published nomenclatonal systems have not accomplished the aims of the work to everyone's satisfaction. Many workers have noted tendencies in previous work to neglect thin but very important lithic as well as time boundaries. Companies have differed as to nomenclature as well as to time relationships of the rocks. Purpose The purpose of this paper is to present a formal system of group and formation names for the lithostratigraphic units encountered in the 'South East Kutai Basin, Kalimantan, Indonesia.
148
We have limited our-selves to the late Oligocene to Recent sediments where, to date, we have production. This work is condensed from the Workshop of Stratigraphic Nomenclature, held on 29 September 1981, in Balikpapan. Five papers on the Stratigraphic Nomenclature in E. Kutai Basin were presented and discussed. This work is pursued upon the recommendations made by the management and governing ooards of Pertamina, and the Stratigraphic Commission of Ikatan Ahli Geologi Indonesia. The writers wish to thank the management of Pertamina, Total Indonesie and Union Oil Co. of Indonesia for their help and encouragement in producing this paper. Location The Kutai Basin straddles the eastern margin of Kalimantan (textfig. 1). The northern boundary is the Mangkalihat Penninsula, to the east is the Makassar Straits Trough, and to the s w t h the Kutai Basin is bounded by the Paternoster Shelf. Geologic History
In the Kutai Basin (text figs. 2 and 3), sediments are known to have been deposited since early Tertiary time, filling the basin progressively from the west toward the east. The area of maximum sediment thickness, the Depocenter, shifted progressively eastward with time, and the maximum thickness of late Miocene to Recent sediments is formed in the offshore portion of the basin (Billman and Kartaadiputra 1974, p. 1). Packages of sediments were formed in a series of deposystems. A cross-section A-A’ on figure 1 can be seen in figure 2. Each deposystem developed a group of formations in a sea regressing to the east. The earliest unit in our discussion is the Pamaluan Formation of Oligo-Miocene age. Bathyal sediments continued to infill the basin until at the top of the unit Outer Neritic sediments are present. In the early to basal
middle Miocene Bebulu Group, the Maruat Formation accumulated in a shallow carbonate shelf, while the Pulau Balang Formation was deposited in Inner to Middle Neritic waters, consisting of more clastic sediments. I n the middle Miocene, the Balikpapan Group Paralic to Deltaic Mentawir Formation was deposited, while the Gelingseh Formation sediments were laid down in Middle Neritic waters with occasional Outer Neritic to Bathyal incursions. At the end of the Balikpapan Group time, an Inner Carbonate Shelf, Reef Shoal sequence was deposited in shallower waters. and a Middle Neritic, low oxygen invimnment was deposited deeper at the time ofthe Nandasan Tongue Member. A break in sediments is noted here, then the Miocene to Pliocene Kampong Baru Group Tanjung Batu deltaic Formation prograded t o the east, while the Sepinggan Formation was deposited in Inner to Middlo Neritic waters, with some shallow carbonate accumulations. At the end d the Pliocene, a lowering of sea level produced a hiatus, especially to the west. During the Pleistocene to Recent still&and, the present Mahakam delta H a n d Dua Formation continued its progradation from the west over the more marine Attaka Formation in the east. Previous Work One of the earliest workers was L.M.R. Rutten (1914) who published notes on the Balikpapan Beds, the Pulau Balang and the Bebulu. 1.M. van der Vlerk and J.H.F. Umbgrove (1927) established the Tertiary Letter Stages Ta to Tf. Later, Umbgrove (1929) added Tg and Th. W. Leupold and I.M. van der Vlerk (1931) published a table of bio-and lithostratigraphic units for the Kutai Basin. In 1943, M.F. Glaessner (pp. 63, 64) summarized the above work, tying the Indo-Pacific Area to European stages. R.M. van Bemmelen (1949, pp 134142) discussed the lithic and paleontologic units of the Kutai Basin. The Stratigraphic Lexicon of Indonesia was
149 issued in 1961 by P. Marks which alphabetically listed units named to that time. C.G. Adams (1 970) revised the Tertiary Letter Stages in accordance with the works of Bolli (1966) and Blow (1969). H.G. Billman and L.W. Kartaadiputra (1 974) published a late Neogene zonation applied to the Offshore Kutai Basin. L. Samuel and S. Muchsin presented a litho-and bio-stratigraphic section of the Kutai Basin in 1975. R. Haak and J.A. Postuma (1975) correlated the Tertiary Letter Stages with the pelagic zones of Blow (1969).
Boundaries The upper boundary of the Pan'aluan Fo:ination is rrpresentzd by limestone beds which are pa; t of the Maruat Formation of the Bebulu G r m p 'T!iere is also an upper contact with the base of the Pulau Balang. The lower boundary is difficult to define lithologically as monotonous mudstoiles and shales also occur in the underlying Oligoccne '--uyu Formation.
Distribution Stratigraphy On textfigures 3 and 4 are summarized the general stratigraphic sequence for the Cenozoic System in the Kutai Basin. The Age, Groups, Formations, Lithology, Seismic markers, and Environment are listed for the lithostratigrapliic units. As the Sea Level Curve demonstrates, the seas were regressive until the latest Pliocene, when a deepening started another cycle in the Recent. STRATOTYPE SECTIONS Type and Hypostratotype sections have been designated for the formations listed here. Where possible, classic type sections have been used. If on examination, many beds are covered or inaccessible, Hypostratotype sections are also designated.
PAMALUAN FORMATION* Name Origin The name Pamaluan was taken from the village of Pamaluan, 30 Km NNW of Balikpapan, East Kalimantan (Leupold and v.d. Vlerk 1931, p. Marks 1961).
*
L.Samuel.
'The Painaluan Formation is exposed over much of the western half of the Kutai Basin, and it also appears at the surface ill the core of some of the most easterly anticlines. The formation has been intersected in some wells drilled onshore and offshore.
Type Section The original type section was mentioned near Pamaluan village but in that locality only the upper Pamaluan is exposed. Hence, the Peringtali Anticline arid Janibu Syncline, located 80 Km NW of Balikpapan, East Kalimantan, are proposed as hypostratotypes of the Pamaluan Formation, see textfig. 7.
Lithologic description
in general, the Pamaluan Formation is represented by light gray to black mudstones and shales with carbonaceous plant remains. The lower Pamaluan consists of massive siltstones and mudstones with occasional thin (1 5 cm), very fine, tight sandstones. The Upper Pamaluan is predominantly mudstone with conchoidal fractures, or bedded shales, often with carbonaceous leaf remains. Sandstone and coal interbeds are also found, and a thin limestone occurs near the top of the formation.
150 Paleontology
PULAU BALANG FORMATION** Name Origin
Globorotalia kugleri, Globigeniza ciperoeilsis, Globorotalia opinuz, Globorotalia izana, Globigerina sellii, Globigerina ampliapertura, Globigerina prasaepis, Uvigerina h ispida, Ra thysip hon sp., Animodiscus spp., Cydammitza spp., Sphaeroiu'ina bulloides. Zones : N 2 - N4.
Tile name of this formation was originally taken from Pulau Balang (Balang Island), an island located approximately 8 Km north-east of the city of Balikpapan in the Balikpapan Bay (Rutten, L.M. 1914).
Enviroiiment
Boundaries
Generally marine, with an Outer Neritic to Bathyal environment of deposition.
The Pulau Balang Formation is a deeper marine unit of the Bebulu Group which is overlying the Pamaluan Formation and underlying the Balikpapari Group, Mentawir and Gelingseh Formations. However this formation shows an inter-fingering relationship with the Maruat limestone Formation. The top of the Pulau Ralang is indicated by the Total Indonesia Co seismic marker, which is traced into the subsurface.
Late Oligocene to early Miocene (N2 - N4).
BEBULU GROUP*
Name Origin The name for this group is derived from Sungai Bebulu, a small creek about 45 Km southeast of Balikpapan, East Kalimantan, Indonesia (Umbgrove 1927, pp 28-41). Leupold and v.d. Vlerk's (1931, p. 614) name of Bebulu beds in part is synonymous with the Bebulu group. The Bebulu as considered by Leupold and v.d. Vlerk above, which consists of marls and limestones, is here placed in the Maruat Formation. Onshore, this formation underlies the Pulau Balang Formation. In places offshore, a portion of the Maruat overlies the Pulau Balang. Both the Pulau Balang and the Maruat Formations are included in the Bebulu Group.
* Sujatmiko ** T. Ismoyowati
Distribution Distribution of the Pulau Balang Formation can be noted onshore (see fig. 6) and offshore in the Total Maruat No. 1 well and Tengah Field. Type Section Type section
: Pulau Balang surface secti-
Location
: Pulau Balang, Balikpapan
Thickness
Bay, 8 Km northeast of Balikpapan, East Kalimantan. :+ 1855 m (6086 feet). -
on (Textfig. 8).
Lithologic description The Pulau Balang Formation consists of interbedded sandstones and siltstones with occa-
151 siona; limestones and claystones. The limestones contain Foraminifera, fragments of Bivalves and Algae in a micritic matrix. The sandstones occur in thin to thick beds with cross bedding and worm burrows. The sandstones are dominantly quartzose, light gray to white, friable to hard, occasionaly calcareous, fine to coarse grained. In the lower part ofthese beds a few thin layers of coal and sand are noted.
Paleontology
Globigerinoides altiapertunts, Globigerinoides difninutus, LepidocJdina ( N ) sitmatrensis, Lepidocyclina ( N ) angulosa, Flosculinella bontangensis, Flosculinella globulosa, Ro bulus inornatus, Bulimina sp, Trochammina sp., Nonion sp., Eponides repandus, Amphistegina papillosa, Brizalina limbata, etc. Zones : N5 - N7 or younger.
cated 42 Km S.S.E. of Balikpapan. The name Maruat is derived from Tanjung hlaruat, a promontory located 50 Km S.S.W. of Balikpapan. Boundaries The upper boundary of the Maruat Formation is placed at the top of the upper carbonate sequence, well defined by the Co seismic marker. The Ralikpapan Group Mentawir Formation and the Gelingseh Formation is found zbove it. The lower boundary is placed at the base of the lower carbonate sequence, usually a fair seismic marker, above the Pamaluan Formation. To the east, in a deeper environment, the more clastic Pulau Balang Formation is encountered. Distribution The Maruat formation can be mapped onshore, East Kalimantan (Textfig. 6). In tfie offshore area, it can be traced seismically throughout the southemmost portion of the East Kutai Basin.
Environment Type Section The lower part of the Pulau Balang Formation onshore was deposited in an lnner Neritic environment with Deltaic - Paralic influence. In the upper part Middle Neritic open marine sediments were deposited.
Coordinates
Early Miocene Te5 possibly higher; N5 - N7 possibly higher.
RTE Water Depth Total Depth Interval
Type well
Thickness
: Total Indonesie--1npex
-
Pertamina Maruat No. 1 (textfig. 9). : 116’ 55’ 22.0” E 1’ 38’ 20.7” S : 9 m (30’) : 42m (1 38’) : 3455m (1 1335’) : 1261m (4137’)-1690m (5545’) : 429m (1408’)
MARUAT FORMATION* Name Origin
Lithologic Description
The name Maruat was taken from Total Indonesie Pertamina Maruat No. 1 well, an offshore exploration well drilled in 1971. It is lo-
The formation consists of two main carbonate sequences at its type locality, consisting of bioclastic calcarenite (reefal facies). These two carbonates are separated by 30m (98’) of interbedded gray shale and fine grained
* Sujatmiko
152 argillaceous sandstone prohabiy bzlongirig to a tongue of the Pulau Balang Poiination (textfig. 9).
this is preoccupied by Rutten (1914), Mohler aid ten Berge (1949) and Luki Samuel (1980). According to the Stratigraphic Code of Indonesia (Suyono 19751, the name Klandasan of Marshall and Schumann is considered a junior synonym to the Mentawir. Boundaries Tlic upper boundary of the Paralic Mentawir is marked by an onlap of the overlying Klandasan Tongue Member of the Gelingseh Formation, represented by the Bu seismic marker of Total lndonesie in the offshore area. The lower boundary is placed at the top of the Bebulu Group Maruat Formation or Pulau Balang Formation, marked by the Cu seismic marker.
hiiro.rrncnt
Shallow Carbonate Shelf. .4gc
Te5 - Tf! (Early Miocenc Miocene)
Early Middle
BALIKPAPAN GROUP1/ Name Origin The name for this group is derived from the town of Balikpapan located on the east coast of East Kalimantan. W. Leupold and I. M. van der Vlerk (1931) called this group as layers, but since "Layers" is not formal stratigraphic terminology (Suyono 1975) it is recommended that this sequence be called a group. The Balikpapan Group is here divided into two formations: the Mentawir Formation and the Gelingseh Formation.
Distribution 'Ihe Mentawir Formation can be mapped onshore, over the southern part of the East Kutai Basin (textfig. 6 ) , and in the offshore by using electric log;. Type Section The Type Section for the Mentawir Formati-
on is at S . Mentawir (Rutten, 1914), 2 3 Km NNW of Balikpapan, East Kalimantan. Many of the sequences are covered by soil, and the Reference Locality below described is here by proposed. Hypostratotype Section
MENTAWIR FORMATION * Name Origin The name Mentawir is taken from the Mentawir river located app. 2 3 Km NNW of Balikpapan town (texfig. 5). This formation was called in 1981 as the Klandasan Formation by Marshall & Schumann (1981, p. 285) but
*
H.Dhanutirto
Location
: Outerops on the beach
behind the Pertamina tennis court near the Banua Patra building and along J1. Minyak in front of Gate I11 Pertamina refinery complex. At Gn. Pancur, outcrops of Mentawir occur in a quarry cut approximately 300 metres south of Pertamina Area
153
Thickness
IV Main Office, Balikpapan, East Kalimantan, Indonesia (textfig. 10). 540 m (1772'). Lithologic description
This formation consists mainly of massive sands and sandstones, white, light gray to brown, fine to medium grained, soft to friable, occasionally interbedded with clays, siltstones and lignite beds. Intercalated with this formation, a number of marls and limestones are found, which possibly belong to the Gelingseh Formation or as discontinuous limestone streaks. Paleontology No guide fossils have been found in the Mentawir Formation. Some benthonic fossils occur, mainly arenaceous forms including Trochammina, ltaplophragrnoides and Ammobaculites. However, the Gelingseh equivalent marls and limestones already discussed above contain Miog.vpsina, Miog),psinoides, Lepidoqvtibia, Flosc~dinella borneensis in the upper portion and Flosculinella bontangensis in the lower portion.
Boundaries The upper boundary of the formation in the Union - Perlamina Sepinggan No. V 1 well is represented by a disconformity of Middle Miocene T f - 2 age. This boundary is a good electric marker, and represents a change from the shales and limestones in the Klandasan Tongue Member above, indicated by the Bo seismic marker of Total lndonesie, to the sands, marls and clays in tile Gelingseh. The lower boundary is placed at the top of the Maruat and Pulau Balang Formation of tile Bebulu Group, and is marked by the 6~ Seismic marker. Distribution The distribution of the Gelingseh formation can be noted onshore in the Klandasan Tongue Member, see below. It is present in the offshore in wells in the Kenndingan and Attaka Fields in the northern Kutai Basin and extends to the Southern portion of Kutai Basin. Type Section Although the Gelingseh was named from S. Gelingseh, no type section was made. It is there fore recommended that the Union Oil Co. of Indonesia - Pertamina Sepinggan No. V--1 well be designated as the Hypstratotype Section for the Gelingseh Formation.
Environment Paralic to Deltaic environment. Age range Middle Miocene Tfl--2 (N9 homotaxy.
(1914) from S. Gelingseh located near Sangkulirang Bay, East Kalimantan.
NI3) by
GELINGSEH FORMATION*
Hypostratotype Sectie ~ Hypostratotype section well
Name Origin Coordinates The name Gelingseh was taken by Rutten * B.B. Sidik
RTE Water Depth
: Union Oil Co. of Indonesia Sepinggan No. V - I (textfig. 11). : Lat 1° 25' 45.54 S [~ng I 160 54' 19.67 E : 31' (9m) KB : 133' (40m)
154 Total Depth Interval
: 11974’ (3650m) : 7,900’ (2408m) to 11,040’
Thickness
: 3,140’ (957m)
(3365m).
Nannoplankton Sphenolithus moriformis, floridanus.
Cyclicargolitus
Lithologic Description Environment The sequences are mainly sandy clay, clay, and thin limestone beds. The general environment of this formation 79007(2408m) Top of the Gelingseh for- is Middle Neritic, with occasionally a transmation. gressive phase bringing in Outer Neritic to 8000’(2438m) Clay/claystone, light gray, Bathyal sediments. soft, occasionally firm, non calcareous; with a Age range little caal, black moderate hard, shiny, brittle. Middle Miocene. 8400’(2560m) Sandstone, white-light gray, very fine to fine grained, moderate sorting, subrounded, friable, occasionally moderately hard; KLANDASAN TONGUE MEMBER* with thin limestone, brown, bioclastic, hard, to Name Origin very hard. 8686’(2647m) Clay, gray to drown, The name Kiandasan was originally derived moderately hard, very slightly calcareous; Inter- from a small creek which flows in the eastern bedded with thin layers of part of Balikpapan town. Muller (1922) gave sandstone, friable, mode- this name to the limestone and marl sequence rately hard, white gray, which can be found at the surface at Gn. Marvery fine to fine grained, koni, Balikpapan, and placed it in the upper grading into siltstone with part of the then named ”Balikpapan Layers”. Leupold and v.d. Vlerk (1931, p. 619) placed carbonaceous material. it in the ”Gelingseh or Upper Balikpapan 10,620’ (3237m) Claystone, light gray to brown, buff, soft to slight- Beds”. The name Klandasan was used by ly firm, slightly calcareous. Marshall and Schumann (1981, p. 285) for 11,040’ (3365m) Bottom of Gelingseh for- another unit, the Mentawir (ut supra p. 13), but this is preoccupied by Muller 1922, Rutten mation. 1927, Mohler and ten Berge (1949) and L. Samuel (1980). According to the Stratigraphic Paleontology Code of Indonesia (Suyono 1975) the Klandasari as used by Marshall and Schumann is a juGloborotalia siakensis, Flosculinella bonra- nior synonym of the Mentawir. ngensis, Globigerinoides cf. altiapertums, Miogypsina sp, Lepidocyclina spp, Miogypsinoides sp. Zones : N9 - N13. * LukiSamuel ’
155 Boundaries
The Klandasan Tongue is a member of the Gelingseh formation of the Balikpapan Group. At the type locality in Gn. Markoni, the Klandasan limestone overlies the Mentawir Formation and underlies the Tanjung Batu Formation of the Kampong Baru Group (textfig. 12). In the Offshore area, this member coincides with the Bo seismic marker as defined by Total Indonesie. Lithologically it changes into mark and shales, and can be distinguished electrically as- well as lithologically from the overlying Sepinggan or Tanjung Batu Formation and the underlying Gelingseh Formation.
Paleontology
Miogypsina spp., Miogypsinoides spp., Lepidocyclina rutteni, Flosculinella borneensis. Down dip : GIobobulimina sp. (pyritized), Bolivina sp., Robulus inornatus. Zone : Tf2, N11 - N13. Environment Onshore : Inner shelf, Reef Shoal carbonates; in the offshore, a Middle Neritic, low oxygen environment. Age : Middle Miocene Tf2.
KAMPONG BARU GROUP* Distribution
Name Origin The Kiandasan Member is well distributed in the southern flank and eastern plunge of Klandasan Anticline, Balikpapan, East Kalimantan. In the northern flank of the anticline, however, only small patches of the limestone are exposed.
Type Section
The KamPong Baru was referred to by LeuPold and van der Vlerk in 1931 (P. 61913 from "Kampong Baru near Samarinda, Kutai District, E.(Kalimantan). This village lies E. of Sanga-Sanga, not to be confounded with another Kampong Baru only 3 Km N. of Balikpapan (where the same beds are out-cropping)". (P. Marks 1961, p. 61). The Kampong Baru Group has two formations, the Tanjung Batu and the Sepinggan Formations.
Gunung Markoni is designated as the Type Section (Muller 1922). It is a hillside about 700 m north of Jalan Markoni at KM 5, southeast of 'Balikpapan Town, East Kalimantan (textfig. TANJ ~ BATU G FORMATION** 12). Along the hill at Gn. Markoni, a 35m thick section of limestone (Sudarjanto 1981) and marls belonging to the Klandasan Member Name Origin is quarried, so the limestone is well exposed, texfig. 12. The proposed name of this formation was taken from Tanjung Batu, a small Peninsula located approximately 4 Km N 338' E of ITCI Jetty, Balikpapan, East Kalimantan. Lithological description Limestone, gray hard, massive, fossiliferous, intercalated with marls.
* **
E. Marks T. Ismoyowati
156 Boundaries
Lithologic description
The Tanjung Batu Formation is a unit of the Kampong Baru Group which overlies the Klandasan Tongue Member of the Balikpapan Group, represented by the Bo seismic marker of Total Indonesie. It underlies the Sepinggan Formation, and in some areas where the latter is removed, the Handil Dua and the Attaka Formations of the Mahakam Group overlie it. Towards the east, the Tanjung Batu Formation makes an inter-fingering contact with the lower part of the Sepinggan Formation.
The type sections of the Tanjung Batu Formation consist of rather different lithologies. Lithologically Section I consists of interbedded shales, clays, siltstones, sands and coals. The sandstones are white to yellowish white in color, composed mainly of frne to medium quartz grains, moderate to well sorted, mostly friable and loose. The sandstones have a channel type geometry and become more shaly toward the margin of the channel. Three cycles of deltaic depositional sequences can be observed along this exposure. Each cycle is distinguished by the existence of coal seams. They are mostly black, lignitic, occasionally friable. Alternation of shales and siltstones can be observed in the small gully, showing current ripples and laminations. In the lower part of this sequence a thin layer of concretions of clayironstone, dark brown, hard, occurs above the sandy clay layers. In Section 11, the sequence which is in laterally the same position as Section l, lithologically consists of clays, shales and coals. The clays are carbonaceous, gray, soft and plastic. The shales occur in thin to thick beds, dark gray, soft and carbonaceous. Thin layers ofsandy clay are noted in the lower part of the sequence. In the upper part, the coal beds occur in very thick sequences. Above these thick coal beds, a hundred foot section is covered by soil, and then in the very upper part laminated sandstone beds occur with intercalated clays and shales.
Distribution The Tanjung Batu Formation can be noted onshore within the bounds of the Kampong Baru Group (textfig. 6). Offshore it is found in wells from Kerindingan Field in the northern part of Kutai Basin to the Total Maruat No. 1 well in the south.
Type Section Type section
: Tanjung Batu surface sec-
tion (textfig. 13). Thickness
15m (Section I) and 57m (Section 11).
:A
+_
Hypostratotype Section Hypostratotype Section Well
: Union Oil Sepinggan S- -1
Coordinates
: Lat 01’ 25’ 47.418” S
(textfig. 14).
RT elevation Water Depth’ Total Depth Interval Thickness
Long 116’ 56’ 0.117”E : 55’ (17m) : 149’ (46m). : 12500’ (381 l m ) : 7520’ to 11308’ (2293m to 3448m) : 3788’ (1 155m)
Paleontology
Trochanzmina arenosa; Textularia agglutinans. Zone
: possibly N13 - - N15 equivalent, by
homotaxy. Environment This formation is almost barren of fauna,
157
only few arenaceous forams being noted. The occurrence of the coal beds suggest paralicdeltaic environment, and also the fining upward of sand grain-size of the sand layers is typical of a channel deposit.
Type Section : Union Oil Co. of Indone-
Type well
sia -Pertamha Sepinggan S- 1, Textfig. 15. : Lat 01’ 25’ 47.418” S Long. 116’ 56’ 00.71 1” E : 55’ (17m) : 149’ (46m) : 12500’ (381 lm) : 1010’ (308m) to 7520’ (2292m) : 6510’(1984m)
Coordinates
RTE Middle Miocene to Pliocene, Tf3-Th equiva- Water Depth lent. Total Depth lnterval SEPINGGAN FORMATION* Thickness Narne Origin
Lithologic description The Sepinggan Formation name is taken from the Sepinggan Field and from the type section, Union Oil Co. of Indonesia Sepinggan S-I. The name $Sepinggan’isderived from Sungai Sepinggan, township of Balikpapan, East Kalimantan.
1010’ - 5000’ (308m -1 524m)
Clays, medium to dark gray, soft, sticky, with thin sands, loose, quartzose, very fine to fine, subangular to subrounded, clear, some thick lignite beds at 1700’. Boundaries limestones, white, hard, 5000’ - 6200’ (1 524m-1890m) crystalline to chalky. The upper boundary is placed at the top of 6200’-6500’ Sands, loose, quartzose, f i e shallow marine shales, sands and carbonates, (1890m- 198 Im) grained, subrounded, clear, just under a lowering of sea level that in some occasional calcareous ceareas left a non-conformable surface above menting, thin limestone which is the Mahakam Group Handil Dua and beds as above, and clays as Attaka Formations. The lower boundary is above. marked by a seismic reflector, the flu marker, 6500’-7520’ Limestones as above, with as defined by Total Indonesie at the Klandasan (1981m-2292m) siltstones, medium brown, Tongue Member of the Gelingseh Formation. medium gray, soft t o firm, The lower Sepinggan Formation lies to the east and sands at base of section, of the deltaic Tanjung Batu Formation, but the loose, fine to medium graiupper part of the Sepinggan overlies the Tanned, subrounded, clear, jung Batu offshore, and onshore where not occasional calcareous ceerosionally removed. menting. Distribution The Sepinggan Formation runs from the south to the north of the Kutai Basin area offshore, and onshore where not erosionally removed.
*
Sujatmiko and E. Marks
7520’ (2292m)
Base of Sepinggan Formation. Paleontology
1010’ (308m)
Late Pliocene Anzrnunia ikebei (Billman and Kartaadiputra 1974,p.305).
I58 1190’ (363m) 1790’ (546m) 5000’ ( I 524m)
7520’ (2292m)
Early Pliocene Asanoina sp (idem) Late Miocene Pseudorofalia catifliformis (idem). Late Miocene Ammonia yabei (idem). Base of Sepinggan Formation.
Zones : N13 - N21 Environments 1010’ (308m) 7520’ (2292m)
Inner to Middle Neritic, Reef-Reef Shoal in part. Base of Sepinggan Formation.
Please note that this formation does not correspond to the pay zones of Handil field. Pays are in the Kampong Barn and Balikpapan Groups. Boundaries The upper limit is the present day sea floor or land surface where it is exposed. The lower boundary is a contact, in places unconformable, with the underlying Kainpong Baru Group Sepinggan Formation or Tanjung Batu Formation. This contact can be seen in seismic sections as a fair marker. Distribution
Age
The western side of the Straits of Makdssar, forming the offshore eastern Kutai Basin, is covered with the Attaka Formation.
Middle Miocene Tf3, N13 equivalent, to late Pliocene Th, N21 equivalent.
Type Section : Union Oit Co. of Indonesia - lnpex - Pertamina Atta-
Type well MAHAKAM GROUP* Name Origin
Coordinates
The name is derived from the Mahakam River, Kutai District, Kalimantan, forming the latest deposystem and contributing its sediments t o this Group. The Mahakam Group has two formations, the Handil Dua and the Attaka formations.
UTE Water Depth Total Depth Interval
ATTAKA FORMATION* Name Origin The formation name, Attaka, is taken from the Attaka field and the Union-lnpex-Pertamina Attaka 1 A well, where it is normally found. This name is derived from the Japanese Atsutaka, meaning Bonanza (Seventy Six, 1973).
*
E.Marks
ka 1A (textfig. 16). 10’ 55.053” S; L,ong. 117’ 38’ 14.665” E : 32’(10m) : 175’ (53m) : I 1660’ (3554m) : 216’ (seafloor) to 1350’ (66m - 41 I m) : 1 134’ (346m) : La1 0’
Thickness
Lithologic Description 2 16’-700’ (66m - 213m)
700’-900’ (21 3m - 274m)
Clays, light greenish gray to medium gray, plastic, slightly calcareous; shell fragments, gastropods, pelecypods; trace glauconite. Lignitic interbeds. Sand, white, pale yellow, clear, angular t o subrounded, medium to coarse, in part very coarse t o pebbly.
I59 Claystone, light olive gray, HANDIL DUA FORMATION * slightly plastic, slightly calcareous. Name Origin 1000’- 1350’ Bioclastics, coralgal, mollus(305m---41lrn) can shells, foraminifera;thin The name Handil Dua was taken from interbeds, Lignite. Handil Dua village, some 80 Km NE of Balik1350’ (411m) Base of Attaka Formation papan and 37km SSE of Samarinda (textfig; 17). This village, which is located in the MahaPaleontology kam Delta, has been chosen by Total Indonesie as its operational base for the Mahakam Delta. Please note that this formation does not Sea floor to 389m (1 19m) No samples. Cdcarih zone (Billman and correspond to the pay zones of Handil field. 389’ to 1350’ (1 19m - 41 lm) Kartaadiputra 1974 p. 305). Pays are in the Kampong Baru and Balikpapan Calcarina calcar, Calcarina Groups. spengleri, Asterorotalia pulBoundaries chella, Pseudorotalia schmeteriana, Pseudorotalia conoiThe Handil Dua Formation, which are modes, Operculina complrmata, Operculina ammonoides, dern marine deltaic sediments formed during Common Pelagics. the last phase of the Holocene Transgression, Globoquadrma humerosa overlies unconfomably the Pliocene 900’-1 350’ (274m-4 11m) N16-bN22 found in this sediments of the Tanjung Batu Formation interval. (textfig. 4). 900’- 1000’ (274111 - 305m)
Distribution
Nannoplankton
910’ (277m) Zones
Coccolithus domnicokfes “17 - “19 (N21-N22) : N22-N23. Environment
Sea floor Sea floor -389’ (66m - 119m) 389’ - 630’ (1 19m - 192m) 630’ - 900’ (192m - 274m) 900’ - 1350’ (274m - 41 lm)
As a Recent sediment, the Handil Dua Formation is developing in a prograding Mahak Delta, comprising approximately 1300 km of predominantly marshy and swampy subaerial delta plain, 1000 km2 of delta front and 2700 km2 of prodelta accumulations (Allen et al, 1979), textfig. 18.
9
216‘ (66m) Middle Neritic No samples Outer Neritic Shallow Marine - Restricted Neritic, Open Marine
Pleistocene to Recent N22 - N23.
Type Sections
In the Mahakam Delta borings S5 and S7 are among a number of shallow (15 to SOm) cored borings which have been chosen as co-type sections (textfigs. 1 7 and 18). In addition, a large number of surface sediment samples were taken from many parts of the Mahakam Delta, situated between 0’ 21’ and l o lo’ South Latitude, and 1170 15’ and 117’ 40’ East Longitude.
*
Sujatmiko
160 Lithological description The Handil Dua Formation is composed of sand, clay, and mud. These sediments are found either in delta plain, delta front or prodelta environments. Paleontology The following foraminiferal assemblages were examined from sea bottom samples taken by a Berthois hand dredge. The samples represent approximately the upper lOcm of sediments. Hyposaline fauna : Hapbphragmodes spp., Trochammina spp., Palmerinella spp. Tidal Marine fauna: ’Fseudoeponides nakanoensis, A s terorotalia trispinosa, EMhidium koeboeensis ”
Marginal Marine fauna : Aeudorotalia spp., Elphidium spp. Shallow Marine fauna: Operculina spp. Environment Mixed Fluvial - Tidal Marine Deltaic System
Age Post - Holocene transgression (SO00 - 7000 years b.p.) (Allen et al, 1979). SUMMARY AND CONCLUSIONS
In summary we have recommended the adoption of the following lithostratigraphic units for use in the Kutai Basin: In the late Oligocene to Early Miocene, the ‘Pamaluan formation; The Early to Middle Miocene Be-
bulu Group divided into the Maruat Formation and the Pulau Balang Formation; The Middle Miocene Balikpapan Group divided into the Mentawir Formation, the Gelingseh Formation, and the Klandasan Tongue Member of the Gelingseh; the Middle Miocene to Late Pliocene Kampong Baru Group consisting of the Tanjung Batu and the Sepinggan Formation, and the Pleistocene to Recent Mahakam Group divided into the Attaka and the Handil Dua Formations. REFERENCES ADAMS, C.G., 1970. A reconsideration of the East Indian letter classification of the Tertiary. Wl. Brit. Mus. (Nat. Hist.) Geol., v.19, no. 3, p. 85-137,3 textfigs, AGUNG, H., 1981. Stratigrafi daerah Pulau Balang, Teluk Balikpapan, Kalimantan Timur. Unpub. Honors paper. Cadjah Mada Univ., Fak. Tek. Jur. Tek. Geol., Yogyakarta. ALLEN, C.P. LAURIER, D. & THOWENIN, J., 1979. Etude se’dimentologique du delta dc la Mahakam. Notes et Memoirs, No. 15, Compagnie Francaise des Petroles, Paris, 156, p., 2 p l . BILLMAN, H. G. & KARXAADIPUTRA, L. W., 1974. Late Tertiary biostratigraphic zonation, Kutai Basin, Offshore, East Kalimantan, Indonesia. Proc. Ind. Petr. Assn. 3d Ann. Conv., p. 301-310. BLOW, W.H., 1968. Late Middle Eocene to Recent planktonic foraminiferal biostratigraphy. Eroc. 1st Internat. Conf. Plankt. Microfossils, p. 199-421. BOLLI, H. M., 1966. Zonation of Cretaceous to Pliocene marine sediments based on planktonic foraminifera. Bol. Informativo Assoc. Venezolana Geol. Min. Petr. v. 9, no. 1,32 p. GLAESSNER, M. F,, 1943. Problems of stratigraphic correlation in the Indo-Pacific Region. Proc. Roy. SOC. Victoria, v. 55 (N.S.) pt. 1, p. 41 -80.
161
HAAK, R. & POSTUMA, J. A, 1975. The rela- MULLER, F. T., 1922. Berichte uber die geotion between the tropical planktonic logische Untersuchung der Klandasan Antiforaminiferal zonation and the Tertiary Minale. B.P.M. Report, unpubl. Far East Letter Classification. Geol. en RUTTEN, L. M. R., 1914. Studien uber ForaMijnb. v. 54,no. 314, p. 195-198. miniferen aus Ost-Asien (Fortsetzung). Geol. Reichs-Mus. Netherlands. INDONESIAN PETR, ASSN., 1974. ~ d k - S-1. Ser. 1, v. 9 (1911 - 1914), no. 4, p. 281papan-Tandjung Field Trip Guidebook, 30-., 5 pl. 324. LEU~OLD,w. & VAN DER v ~ m1. ,M., SAMUEL, L., 1980. Pengaruh Kegiatan Perminyakan Terhadap Geologi Tatalingkungan 1931. The Tertiary. In Festbundel K. MarKota Balikpapan. Jour. Ikatan Ahli Geolotin, Leidsche Geol. Meded., v.5, p t . 3 , ~ . gy, Indonesia, June, 1980, 6 fgs. 611-650. ----& MUCHSIN, S., 1975. Stratigraphy MARKS, P., 1961A. Stratigraphic Lexicon of and sedimentation in the Kutai Basin, KdiIndonesia, Rep. Indonesia Kement. Perekon. Pusat Djawat. Geol. Bandung, Publ. Keilm. Ind- Petr. 4th An. Conv. p. 27-39. No. 31, Ser. Geol., 233 p- 6 pls. 1961B. ~ dstratigraphic ~ , hxicon SEVENTY SIX, 1973. Attaka means bonanza. of Indonesia. Rep. Indonesia Kement. Seventy six, March, p- 14perekon. pusat DjaWat. ~ ~ Bandung. ~ 1 SUDARJANTO, . 198 1. Stratigrafi batubara dan batugamping daerah Balkpapan Timur* unh b l . K e h . no. 31 A, Ser. Geol. 135 p., 1 pub. Honors paper, Gadjah Mada Univ., PiFak. Tek. Jur, Tek. Geol., Yogyakarta. MARSHALL, A. J. & SCHUMANN, H. O., 198 1. Stratigraphy and Hydroarbon poten- SUYONO MARTODJOJO, 1975- Stratigraphic ti4 of the Beds in the Kutei BaCode Of Indonesia. lkatafl Ahli Geologi Indonesia, l9 P. sin, East Kalimantan, Indonesia. Proc. Ind. Petr. h s n - 10th Ann. Conv. p. 285 - 295. UMBGROVE, J.H. F., 1927- Neogene forminiferen van de Soengai Beboeloe, Pasir, MOHLER, W. A*, 1943, Palaeontology and Stratigraphy of the ti^^ of SJ. B ~ Zuidoost-Borneo. ~ ~ ~ Wetensch. ~ . Meded. Dienst. Unpubl. Rep't., Chishitsuchosajo. Bandung, Mijnb- Ned. Indie-v.5, Pa 28-4112 p, 4 PIS. ., 1929. Tertiary sea connections between Europe and the Indo-Pacific area. MOHLER, W. A. &TEN BERCE, J.R.J., 1949. Palaeontologisch onderzoek Mentawir en Proc. 4th Pacif. Sci. Congr. Jawa (reprint standardsectie Klandasan. Unpubl. Rep't, p. 1-14). B. P. M. Report, no. 10415,20 p. VAN BEMMELEN, KW., 1949. Geology of MUGNIOT, J. F., 1981. Seismic facies interIndonesia, p. 126-142, &art p. 139. pretation, a contribution to the stratigraphi- VAN DER VLERK, I.M. & UMBGROVE, J.H. cal framework of the Mahakam Delta, F., 1927. Tertiare gids foraminiferen van Workshop on Strat. Nomencl. in East Kutai Nederlandsche Oost-Indie. Wetensch. MeBasin, Kalimantan, 8 p., 8 fgs. ded., vol. 6,35 p.
162
imj
Pre-Tertiary Basement
..........
1 0 0 0 F t . Bathymetric
MAJOR STRUCTURAL ELEMENTS OF KALIMANTAN
Contour Km.
Figure 1
163
DIAGRAMMATIC CROSS-SECTION A --A' KUTAI
BASIN FIGURE
h
0
SANDSTONE LIMESTONE
0
1
SHALE BASEMENT
f
I
164
DIAGRAMMATIC STRATIGRAPHIC SUCCESSION SOUTH EAST KUTAl BASIN EAST KALIMANTAN INDONESIA
-
FIGURE 3
AGE PLEIST TO RECENT
"CIOCENE
LATE MIOCENE
-
.-........... .. .. .. .... ... ...
GROUP
MIDDLE MIOCENE ? Tft
x vouMcn
....... MIODLE MIOCENE
EARLY MIOCENE Te 5
N4 EARLY MIOCENE LATE 3LIGOCENI LEGEND
0:,"n", B
liqnite
silts
@ limestone
shale
-a- Seismic
Marker
165
. LITHO -AND BIO - STRATIGRAPHY SOUTH EAST KUTAI BASIN EAST KALIMANTAN INDONESIA
-
FIGURE 4 L
I
BENTHONIC
.
I QUATERNAR)
N 23/22
Q
LOCALZONES
CALCARINA
LATE
I
I
I
LlTHO UNIT PROPOSED
GROUP
FORMATIONS
/ MERS
MAHAKAM GROUP
I
\MMONIA IKCEEI
N 21
W
z
N 20
W V
I!
Th :ARL'
N 19
-
N 18
ASANOINA
-I
a
~
S CATILLIFORMIS
N 17 LATE
--
N 16
Tg
N 15
N 14
Tf 3
FM
N 12 WDDL
~
z
TANJUNG B A T U
N 13
W
AMMONIA YABEIl
Tf2
N II
2
w 0 0
2
MARUAT EARL'
LATE OLIGOCENE
Te 5
PULAUBALANG
r ; PAMALUAN
FM
166
167
I
FIG. 6
DISTRIBUTION OF GROUPS
MAHAKAM GROUP KAYPUNG BARU BROUP
n
BALMPAPAM O R O ~ P
168
TYPE
SECTION
PRlNGTALl AND JAMBU SURFACE SECTIONS
PAMALUAN FORMATION FIGURE 7 HICKNESS
AGE
m
a & -
E W I
L
YL
g 0
0' c
ENVIRONMENT
DESCRIPTIONS
-I
Iz
g
z
=
c
ANG
OOO.
Mudstone with conchoidal fractures or bedded shales, often with carbonaceous leaf remains. Sandstone and coal beds are also found. Thin limestone occurs near the top o f the formation.
iooo
Groy to block shales with no visible
plant fragments. Interbedded with medium groined sandstone up to ( 5 m thick
TUYU FORMATION
I
TYPE
SECTION
B A L A N G I S L A N D SURFACE S E C T I O N
P U L A U BALANG FORMATION THICKNESS
I
v)
S
L
L i w
FIGURE
. ! I -1
ENVIR(
r
DESCRIPTIONS
W
5 6
I ' L
hard, occosionally calcareous, f l n e t o coarse grained, q u a r t z -
ose sondstones. The sandstones occur i n thin t o thick beds with cross bedding and worm burrows.
Interbedded
with the sandstones ore thin t o moderately thick beds of dark gray, occasional;y
carbonaceous, calca
-
reous, siltstones and claystones. In the upper part of the column ore 1.2
- 2.
2 m., white t o tan,
massive, fossiliferous limestones.
O t
-
- L
Z
Q
"
C
o
Light gray t o white, friable t o -
=
m
170
TYPE
SECTION TOTAL INDONESIE - INPEX - PERTAMINA MARUAT No.1 MARUAT FORMATION z 0
DEPTH
e
AGE
fr
B
MENT,
IIR F M
z 0 I-
a
z
UPPER
U
LIMESTONE
0 LL
I-
% ! U a z
PULA1
PUL4U BALANG FY
LOWER
LIMESTONE
BALANG FM
F EINE T (METERS)
2 t-
1 1
E N V l RONMENT
D E S C R I P T I0 N S -ikI;~ $ Ef 4 !$( O W
"2
171
HYPOSTRATOTYPE SECTION BALIKPAPAN SURFACE SECTION
MENTAW IR
F 0 R M A TlON FIGURE 10
ITHICKNESS
E l
II
4
DESCRIPTIONS
0
I
t
-
3
(LANDASAN TONGUE MBR. 500
----_.......... ----
................. ---- 1650 ------eoe ---
-.
......... ........ ........ --........ ........ __.___
-
3 5
400 --I320
0 W ZOO
-- too0
!2 z I
200 - - 6 6 0
a,
z
......... .. .. .. .. .. .. .. ..
........
coarse grained.
f.-.:... ? -.........
cross bedding
....... .........-. ......... ......... ......... -. . ..... ........ ... ......... ..... .. .. .. .........
TH
........ ........ .......
P U L A U B A L A N G FM.
lnterbadded with the sandstones ore thin to medium lignite layers, clays
'003
.......
........ ......... ......... ....... ...............
.WE% UNKNOWI
The sandstones occur in thin to very
1 ---leo, .........
-
Sandrtones, quortzore, white, l i h t gray
to brownish, soft to friable, fine to
. .. ._.. . -.......~ -.. .....-........-. - B o a ............... . .. .-.. . .. .. ... - a 0 6
--........ 100 --330
"'
802
and siltstoner
in t h e upper part.
ENVIRONMENT z
172
HYPOSTRATOTYPE SECTION UNION - PERTAMINA SEPINGGAN V
-1
G EL I N G S E H FOR MATI 0 N FIGURE I 1 f,
5
U
E
AGE
LANDASAN TONGUE MBR
ENVIRONMENT
$
DEPTH IN FEET (METERS)
0 2
0ESCRIPTIONS
I
L
Clay .claystone,liqht pray ,soft .occasionally firm non coRareous,with l i l t l e coal, black moderate hard, brittle, shiny. Sandstones,while light gray,very fine to fine grained ,mod sorting rubrounded,friable. occortonatly mod hard with thin limestone brown, bioclostic.hord
rr) c
z I
g ; z m Y
f
1
$ % u s Ec zE k g
Clay .pray to brown, moderate hard, ver y
(3,
slightly c o k a r e o u f
z
lnlerbedded with thm layers sandstone, whlte9ray.very fine to fine proined.prading to siltstone with carboniferous moteriol
-
Cloyrlone, light pray brown. b u f f , soft to slightly firm,rlightly calcareaus. Interbedded wtlh l h i n layers sendstone,
4
m n
0
-
U
a
Tf
MIDDLE
2
P
N
MIOCENE
s
1
1
:: -
KLANDASAN TONGUE MBR
I I
T
n
C
z
:1 c
-40
174
I-!
w =
-
m
lN3lVAlIIO3
91
-
E41
3 ~ 3 3 0 1m ~a a i w NOllVWMOj
n1V9
SNIIPNVI'
175
HY POSTRATOTYPE SECTION UNION
- PERTAMINA
SEPINGGAN S - 1
TANJUNG BATU FORMATION
' E 2
AGE
SEPlNGGAl
z
0 I4
= a w
O Z LL
0
0
-
= r I4
co
W
c3
I4
z - 1 => 7
z a I-
KLANDASAN TON
0
F IENE T (METERS)
2
5
DESCRIPTIONS
176
TYPE
SECTION
UNION-PERTAMINA
SEPINGGAN S - I
SEPINGGAN F O R M A T I O N
Cloys medium to dark p r a y , s o t l , ~ l t c h y;
with thin sands,loose,quarliose.~~ryfine
lo fine qratnad.subonpulor lo subrouded, clear.lOme thin l i p n i l 0 beds 0 1 1700'
L i m e s l o n e s , w h i l e . hord.cryrlolline l o chnlky
i 57
-
I
TYPE
UNION INPEX
SECTION
- PERTAMINA ATTAKA
IA
A T T A K A FORMATION FlGUl IE 16 DEPTH
z
0 I-
a
I cc
2
AGE
IN
FEET (METERS)
ss
E N VIRONMENT
0 E S C RIP T I 0 N S
C 2
Colcorina
nite, lignitic interbeds. Sond,white, pole yellow, cleor angular to subroundrd, medium to coarsetin port very coarse to pebbly. Bioclostics ,corolgal ,molluscon shells,forominifera thin interbeds lignite.
,
WAKA FIELD
n
178
T Y P E CORE
SECTION S-5/B1
HANDIL DUA F O R M A T I O N DEPTH
AGE
I-
y
:
ENVIRONMENT
3 e c1 -
0ESCRIPTIONS
s w
+ J
c
0
-1
-
a * c ’
8 :+’ s
4ND SURFACE
c z
W
0 W
a I W
z lLl
SE NOT
2!!izLL BALlKPAPAW
179
TYPE SECTION CORE S-7 HANDIL DUA FORMATION FIGURE
L A N D SURFACE I---+
Sands, clayey
, clays. dark
gray plant remains
Sands, f i n e grained, g r a y , clayey.
I - *
C l a y s , g r a y , lenlicular
W
Clays,gray,with lenses o f sand and silt5
z
0 W
a I Sands, very fine . c l a y e y , w i t h lenses Of silty clays
W
z w
u 0 -I
0 I
Clays, g r a y , with horizontal laminations, Plant remains, abundant bioturbations and shell fragments ~~
.. . .. . . . . .
..-.. .. . .. -----
8ASE NOT R
\
i.
18
