Pleistocene formations are in a separate file
INDEX
Old Andesite Fm., Oostingh's molluscan stratigraphy of the Neogene, Orbitoiden formatie or Orbitoiden Kalk (or OK), Oudste schieferformatie, Oyo Beds, Parigi lst, Pelang Beds, Pemali Beds, Penyatan Beds, Platten Member, Preanguerian Stage, Prupuh Kalk, Rajamandala limestone, Rambatan Beds, Reef limestone facies, Rembang Beds, Rembangian Stage
OLD ANDESITE FORMATION (Oude Andesieten) Oligo-Miocene
Verbek (R.D.M.), Fennema (R.) (1896). Geologische Beschrijving van Java en Madoera, vol. I & II.
The authors originally conceived of a Lower Miocene volcanic "cycle", during which large andesitic and basaltic volcanoes were formed. Afterwards conglomerates, breccias and sandstones were supposed to be formed as a result of the erosion of this volcanic system. While even later clays, marls and limestone were formed in marine surroundings.
A second volcanic cycle presumably started after the marine limestone stage, which lasts till recent times. The difference of the "Old" Andesite Formation and the "Young" Andesites was mainly based on geomorphological appearances: the young andesites forming part of the distinct strato-volcanos, while to the Old Andesites were ascribed the leveled ruins. Also the authors assumed that the Old Andesites were erupted along fissures instead of forming cone-shaped strato-volcanos.
As a result, many upper Tertiary and Pleistocene andesitic deposits were ascribed to the lower Miocene Old Andesite Formation (e.g. those of the Kendeng Hills: the Notopuro - Jombang Layers, etc.). According to the editor the term is badly defined, and should be rejected, or defined anew.
However, the term has been reintroduced by Westerveld (1941) and van Bemmelen (1949a, pp. 117, 119, 124, 184, 596, 715) mainly for deposits of upper Paleogene and lower Miocene andesitic volcanism in South Sumatra, forming the base of the Neogene sedimentation, and possibly equivalent to the Lahat Formation.
Such middle Tertiary volcanic activity may be recognized in many parts of the archipelago: Java, Sumatra, Celebes, New Guinea, etc. As such the term retains its use, and may be preferred to purely local names.
OOSTINGH'S MOLLUSCAN STRATIGRAPHY OF THE NEOGENE
Oostingh (C.H.) (1938). Mollusken als gidsfossielen voor het Neogeen in Nederiandsch Indic. Handelingen van het achtste Ned.-lnd. Natuurw. Congres te Soerabaya, pp. 508-516.
Acomparative study of the molluscan faunae of the Tertiary, especially those from Java, has led the above-mentioned author to distinguish a number of stages, which are characterized by specific gastropoda. The subdivision thus made has no pretensions to be definite, and may be considerably extended as fieldwork and research proceeds. The stratigraphy is as follows (going downward).
Bantamien, type locality Bojong (on the road from Malimping to Pandeglang), name derived from Residency Bantam,. W Java. Formations in this stage: Bojong Formation, Cikeusik Formation in W Java; Lignitiferous Formation, Operculina Sandstone Formation, Fossiliferous Marl and Sandstone Formation in N Sumatra, Palembang Formation pp. in South Sumatra. About equivalent to Lower Pleistocene of Europe.
Fossils: Turritella angula bantamensis, Clavus malingpingensis.
Sondien, type locality Cilegong (on road from Malingping to Pandeglang), name derived from Sunda. Formations in this stage: Cilegong Formation, Cimanceuri Formation in W. Java, Sonde Formation in East Java, Fufa Formation of Seram, etc.
Fossils: Turritella angulata bantamensis-tjicumpaensis, Terebra verbeeki, T. insulindae, Conus condeianus.
Approx. equivalent to Upper Pliocene (T. h2).
Cheribonian: type locality Cijurey near Cheribon, N Central Java. Formations in this stage: Cipacar Formation, Menengteng Canyon Formation, etc.
Fossils: Turritella angulata acuticarinata.
Approx. equivalent to Lr. Pliocene.
Ciodeng stage. (Not definitely named as the faunae are still insufficiently studied). Type locality: Kramat, W. Priangan. W Java. Formations belonging to the stage: Genteng Formation, Cimandiri Group, Ciodeng Formation.
Fossils: Turritella angulata cramatensis.
Approx. equivalent to Upper Miocene (T. g.).
Preanguerian, type locality Citalahab near Njalindung, W Java. Named after the Priangan (Preanger), a part of W Java. Formations in this stage: Bodongmanik Formation; Cilanang Formation; Njalindung Formation; Cidadap Formation; Lower Palembang Formation; Gelingseh Formation, in Borneo; Kama Formation in Burma.
Fossils: Turritella angulata angulata, Siphocyprea caputviperae, Vicarya verneuili callosa.
Approx. equivalent to Middle Miocene (T. f2-3).
Rembangian, type locality Sedan near Rembang, N coast Central Java. Formations in this stage: Rembang Formation, West Progo Formation.
Fossils: Turritella subiulata.
Approx. equivalent to Lower Miocene (T. e5-f1).
References: Oostingh (C.H.) (1935): Oostingh (C.H.) (1938 & 1939) Bemmelen (R.W. van) (1949a), pp. 82, 83, 108.
OUDSTE SCHIEFERFORMATIE Mesozoic (Karimondjawa Islands).
See: Karimunjawa Slates.
P
PACALAN LIMESTONE HORIZON (Formation) (Patjalan kalksteenzone) U. Pliocene
Bemmelen (R.W. van) 1938). De Ringgit-Beser. Nal. Tijdschrift. van Ned. Ind., vol. 98, pp. 171-194.
Neritic marine limestones, possibly laterally passing into the Menuran layers .
They are conformably overlain by the Leprak formation. The base of the limestones is unknown.
Type locality: Pacalan, 2 km S of Situbondo, N part of East Java.
Geographical distribution: Area of a few square km around type locality only.
Reference: Bemmelen (R.W. van) (1949a), p. 552.
OYO BEDS (Formation) (Ojo lagen) Miocene
See: Southern Mountains Miocene.
PELANG BEDS (Formation) Miocene
Bemmelen (R.W. van) (1949). The Geology of Indonesia, vol. IA, p. 572.
Strongly crushed gray marly mudstone with lenticular intercalations of limestone with large Eulepidina (diam. 10 mm).
These layers form the base of a Neogene series typical for the Western part of the Kendeng Hills. They are overlain by the Kerek Beds. According to van Bemmelen the Pelang Beds are equivalent to the Lutut Beds and the Sigugur limestones, the former occurring in the vicinity of Semarang, the latter in the Karangkobar area.
Type locality: About 1 km South of Juwangi, near Kedungjati, residency of Semarang, Central Java.
Geographical distribution: Type locality, and small limestone hill of Mrisi in the N-part of the Western Kendeng (C. Java).
Diagnostic fossils: Eulepidina sp.
Recent searches have been unable to find the outcrop called "small limestone hill of Mrisi" even thought there is only one village of this name in the area indicated. Around this village only hills of Kapung limestone have been found (1999). The Pelang Beds have excellent Td faunas of mixed Nummulites fichteli-intermedius, Eulepidina and other larger forams, with no hint of reworking. The intecalated grey marls are mid Oligocene with rich planktonic foraminifera and nannofossil assemblages indicating and age in zone NP 24.
PEMALI BEDS (Formation) (Pemali serie) Miocene
Haar (C. ter) (1934). Toelichting bij Blad 58 (Boemiajoe), Geol. kaart van Java, 1 / 100,000, pp. 10- 12.
Grey-blue and gray-green, rarely well-bedded Globigerina-marls, with sparse intercalations of grey-blue sandy limestone beds. Along Cisadap river white tuffoid sandstone and coarse sandstone lenses occur, the latter containing Foraminifera. The beds are very monotonous, and at least 900 m thick. In the type region the underlying strata are not disclosed.
The beds may according to van Bemmelen be correlated with the Merawu Formation in the Karangkobar region which disconformably overlies the Eocene in that region. Apart from the foraminifera mentioned below, which indicate a middle Miocene (T. f) age, Nummulites djogjakartae was found, no doubt from reworked Eocene deposits, which therefore cannot be far down below the lowest known parts of the Pemali Beds. Also according to van Bemmelen, the Pemali Beds may be correlated with the Kerek Beds and the Rembang Beds in East-Java, and the Annulatus Formation in W Java.
The Pemali Formation is overlain by the Rambatan Formation.
Type locality: The beds are named after the Kali Pemali (Pemali river) which runs W and N of Bumiaju, South of Cirebon (Cheribon), C. Java. The true type locality, however, is a section along Cibabakan (Babakan River), long. 108° 52' 57" E, lat. 7° 1' S in the NW corner of sheet 58, Geol. Map of Java, 1 / 100,000.
Geographical distribution: Sheets 58 and 54, Java Geol. Surv., Western section of N Serayu Range, and to the W as far as the Bogor area and Bantam.
Diagnostic fossils: Trybliolepidina aff. rutteni van der Vlerk; Nephrolepidina martini Schlumberger; N. ferreroi Provale Miogypsina sp. Cycloclypeus ex gr. C. carpenteri; Katacycloclypeus sp. from sheet 54 Trybliolepidina radiata Martin.
References: Hetzel (W.H.) (1935), pp. 11-13; Bemmelen (R.W. van) (1949a), p. 604.
In June 2001 a visit was made to the type locality of the Pemali Beds by Peter Lunt (Coparex) and Gerry Burgon (Gulf). From GPS locations and using Ter Haar's maps, cross-checked with several landmarks, we are confident the correct location was found. Also the samples were widely spaced, 1.6 kms N-S, and have been plotted over Ter Haar' map. Several samples of green-grey mudstone were taken and all these proved to be of Early Pliocene age. Well preserved planktonic faunas include Globorotalia tumida, exclusively sinistrally coiled Pulleniatina spp., Globoquadrina altispira, Sphaeroidinella dehiscens -but not the well developed forms of Bandy, and occasional Globorotalia margaritae. The environment of deposition was deep marine. One sample contained abraded Amphistegina.
The implications of this age assignment are considerable, if all location mapped as "Pemali" are a single formation, not least being the question of what land mass was uplifted to source the Eocene and Early Miocene larger foram bioclasts. Note, the sample of Ter Haar that yielded the larger foram assemblage, including the Nummulites djogjakartae was in a nearby tributary of the Cibabakan River, about 800 m west of some of our samples, in a lens of sand.
PENYATAN BEDS (Formation) (Penjatan serie) Miocene
Bemmelen (R.W. van) (1937). Toelichting bij Blad 66 (Karangkobar), Geol. kaart van Java, 1/100 000, pp. 13-16.
The Penyatan Formation overlies conformably the Merawu Formation, while the limit with the latter is difficult to define exactly. It is distinguished from the Merawu Formation by: a) the absence of quartzose elastic beds, b) the presence of increased andesitic volcanic beds. Lower-, Middle- and Upper Penyatan Formation have been distinguished.
1. The Lower Penyatan Formation. Marly tuff-sandstones and coarse to fine tuff breccias (augite and augite-hornblende andesites), containing Globigerina and other smaller foraminifera, indicating a marine deposition.
The thickness, as well as the coarseness is very variable. In sheet 66 the thickness varies from 200 m in the S, to 500 m in the north. Chlorite, sericite, serpentine and zeolites indicate hydrothermal changes.
2. The Middle Penyatan Formation is distinguished by the presence of andesitic and basaltic lava-flows. These flows are submarine, and the composition is for a large part of glass, indicating quick cooling. Between the flows lenses of Globigerina-marls occur.
Further constituents of the Middle Penyatan Beds are breccias and agglomerates and tuff-sandstones. The beds are very resistant to erosion, and tend to form ridges in the field. The thickness is variable, as the beds in fact only represent a strongly volcanic facies. In the Western Part of the East-N Serayu Mnts (sheet 66) the thickness of this particular member varies between 2,000 m in the W to a few meters in the East. More to the East, S of Semarang (sheets 73-74) the thickness varies from 1,000 m in the S to zero in the N. The eruption-centra must probably be sought in the S.
3. The Upper Penyatan Formation. Globigerina-containing tuffaceous marls, clays and andesitic tuffs, without coarse components or lava-flows. The thickness is about 700 m in the West (sheet 66) diminishing to almost zero in the East (sheets 73-74). The reduction in Eastern direction is probably due to an orogenic movement, which started first in the East, and which caused the sediments to be eroded away in part. In the, East, the Banyak Beds overlie the Upper Penyatan Formation with a distinct disconformity, while in the West, the disconformity with the overlying Bodas Beds is hardly perceptible, if at all present.
No fossils indicating an age have been mentioned. The underlying Merawu Beds are of T. e.-T.f. age, the overlying Bodas Beds contain some larger Foraminifera indicating a probable Uppermost Miocene age. Therefore the Penyatan Beds must still be included in the T. f.
Type locality: Kali Penyatan (river), which cuts through the beds over a considerable distance. The K. Penyatan joins the Gintung R. at a point long 109° 34' 27" E, lat. 7° 17' 40" S.
Geographical distribution: Eastern Part of the N Serayu Range, S of the towns Pekalongan and Semarang, N Central Java; mapped distribution in the SW corner of sheet 66 (near Purbolinggo) and in sheets 74-73.
References: Bemmelen (R.W. van) (1941), pp. 24-27; Bemmelen (R.W. van) (1949a), p. 605.
PREANGUERIAN (or PREANGERIAN ?) STAGE Miocene
See: Oostingih's Molluscan Stratigraphy of the Neogene.
Q
R
RAJAMANDALA LIMESTONE (Formation) (Radjamandala Kalk-steine) Oligo-Miocene
Martin (K.) (191 lb).Vorlaufiger Bericht bber geologische Forschungen auf Java. Zweiter Theil. Samml. d. geol. Reichsmus, Leiden, serie 1, Bd IX, pt. 4, pp. 24-28, 56.
About 200 m thick, massive, corailine limestones forming a marked ridge near Rajamandala, about 50 km West of Bandung, West Java. The beds overlie marly clay-shales and quartz-sandstones with Nummulites fichteli-intermedius of [early] Oligocene age, and are in turn overlain by Globigerina marls and andesites with marine intercalations of Burdigalian age. The fauna included in the limestones is of Aquitanian age. The limestones are strongly disturbed by tectonical movements, partly overthrust.
Other names: Masigit limestone, van Bemmelen, 1949, pp. 109, 639; Tagogapu limestone, Leupold & van der Vlerk, 193 1, pp. 639 and table
Type locality Gunung Masigit, near Rajamandala-Cianjur, Preanger, West Java.
Geographical distribution: Near type locality only.
References: Harting (A.) (1929), pp. 1-14; Kuper (H.) (1931), pp. 105-109; Bemmelen (R.W. van) (1949), pp. 109, 639; Leupold (W.) and Vlerk (I.M. v.d.) (1931), pp. 639, table.
RAMBATAN BEDS (Formation) (Rambatan Serie) Miocene
Haar (C. ter) (1934). Toelichting bij blad 58 (Boemiajoe). Geol. Kaart van Java, 1: 100,000, pp. 12-15.
The base consists of calcareous sandstones and conglomerates alternating with marls and shales in thin layers. It is probable that an erosion-hiatus consists between the Rambatan Beds and the underlying Pemali Beds as fragments of the latter beds are contained in the conglomerates. On top of these basal beds are lying thin-bedded calcareous sandstones, light grey to blueish coloured. The bedding planes are often corrugated. Intercalated between the sandstones are thin layers of marl. The clastic part of the calcareous sandstones consists of andesitic material, increasing in relative [abundance] towards the South. Typical for the sandstones is the presence of fibrous calcite in thin layers, the fibres standing at right angles to the bedding planes, The beds contain numerous foraminifera, listed below. The fauna points to a middle miocene age (T. f2-3). The total thickness of the beds is 300 m. The Rambatan Beds overlie the Pemali Beds and are overlain by the Lawak Beds. According to Van Bemmelen (1949), p. 605) the complex Rambatan, Lawak and Halang Beds may be correlated with the Penyatan Series in the Eastern part of the North Serayu Range.
Type locality: The formation is named after the Kali Rambatan, whicii over a distance of about 10 km flows along the contact between Rambatan Series and Halang Series. The best section is found where the Rambatan River cuts through the anticline 1 km SW of Pamulian, long. 108° 54' E, lat. 7° 31' 30" E.
Geographical fossils: Cycloclypeus inornatus var. indopacifica Tan; C. radiatus Tan; Trybliolepidina rutteni van der Vlerk; Nephrolepidina ferreroi Provale; N. angulosa Provale; Miogypsina thecidaeformis Rutten Gypsina globula (Reuss).
References: Hetzel (W.H.) (1935), pp. 13, 14; Bemmelen (R.W. van) (1949a), pp. 605.
REEF LIMESTONE FACIES (Member) (Rifkalk facies) Miocene
See: Cimandiri Complex.
REMBANG BEDS (Formation) (Rembang lagen) Miocene
Martin (K.) (1900). Samml. d. geol. Reichsmus. Leiden, ser. 1, vol. 6, pp. 173-174.
Limestones and marls reaching a thickness of over 3,000 m, containing faunas of Mollusca and larger Foraminifera. Martin found that the molluscan fauna contained 15 % of recent forms, indicating a Lower Miocene age (Martin, 1907). Recent studies (Haanstsa and Spieker, 1932; Waner and Hahn, 1938; Pannekoek, 1936) have furnished 212 species determined from the Rembang Beds, 40 of which were found to belong to recent fauna, i.e. 19 %. From this a Lower Miocene (Burdigalian) age was concluded (Rembangian Of Oostingh).
In the Cepu area (B.P.M.) a tripartition is found
3. Upper orbitoid limestone,
2. Lower orbitoid limestone,
1. Base Marl,
with ages Tf2, Tfl and Te respectively. The very thick Base Marl is correlated with the Kujung formation and considered to be a Gumai tectofacies unit.
The base of the Rembang Formation is unknown, even from drillings by the B.P.M. The beds are overlain by the Wonocolo Stage of the Cepu Tertiary section.
Type locality: Rembang, NE Java.
Geographical distribution: Residency of Rembang, Cepu area, W. of Surabaya, NE Java, in the areas of numerous anticlines. Size of area: 200 km in E-W direction, 65 km in N-S direction.
Diagnostic fossils: Lepidocyclina (Eulepidina) sp.; Cycloclypeus annulatus.
References: Martin (K.) (1932), pp. 149-161; Haanstra (U.) and Spieker (E.) (1932); Wanner (J.) and Hahn (E.) (1935); Pannekoek (A.) (1936); Schuppli (H.M.) (1946), pp. 1-22; Schuppli (H.M.) (1932), pp. 95-121; Bemmelen (R.W. van) (1 949a), pp. 586, 587; (1 949a), p. 33, table 5.