Definitions of Pre-Pleistocene formation names in Java

Pleistocene formations are in a separate file

INDEX

Cadasngampar Beds, Candi Beds, Cheribonian stage, Cidadap Beds, Cijengkol Layers, Cijurei Beds, Ciguha limestones, Ciherang Beds, Cijajar Beds, Cijulang Beds, Cikeusik Beds, Cilanang Beds, Cilegong Beds, Ciletuh Beds, Cimanceuri Beds, Cimandiri Complex, Cimapag Beds, Ciodeng Beds, Ciodeng Stage, Cipacar Beds, Cipluk Beds, Cisande limestone, Citalang Beds, Citarate Beds, Citarucup Layers, Citarum Beds, Crystalline schists

CADASNGAMPAR BEDS (Formation) (Schichten von Tjadasngampar) Miocene

Martin (K.) (1900a), Die Eintheilung der versteinerungsfuehrende Sedimente von Java, Samml. d. Geol. Reichmus. Leiden, ser. 1, vol. 6, pts 3, 4, pp. 162-164.

Insufficiently defined sediments from the upper Tertiary of West Java.

The molluscan fauna contains 27 % recent species and is regarded by Martin as of upper Miocene age. (Martin, 1919).

Type locality: Cadasngampar, SE Preanger, West Java.

Geographical distribution: Similar molluscan faunae were described by Martin from Selaceu, Parungponteng, Cilintung, all in SE Preanger.

References: Martin (K.) (1919), pp. 129-130.

Martin (K.) (1913). Einige allgemeinere Betrachtungen ueber das Tertiaer von Java. Geol. Rundschau, vol. IV, pp. 164, 169.

Insufficiently defined marine marls with rich fossil fauna of molluscs. The marls contain 51 % recent forms, and are regarded by Martin as of Pliocene age (Martin, 1919). Quite probably this marl formation is identical with the Kalibiuk formation and the name Candi formation is to be considered as obsolete.

Type locality: Candi, near Semarang, North Central Java.

Geographical distribution: Not established.

Other name: Gunung Gombel Beds. Reference: Martin (K.) (1919), pp. 29, 133.

Oostingh (C.H.) (1933). Neue Mollusken aus dem Pliozan von Java, De Mijningenieur, vol XIV, p. 213.

Oostingh's Cheribonian stage of the Pliocene (Lower Pliocene) comprises a number of fossiliferous sediments characterized by a certain molluscan fauna (see below). These are the "Turritella beds" from Bentarsari, near Tegal, Cijurei Beds near Cirebon, Cipacar Beds in Bantam, W Java, the Waled Beds, etc. In a later publication Oostingh (1936, 1938) added more stages of Miocene and Pliocene, distinguished by molluscan faunae (see Oostingh's Molluscan Stratigraphy of Neogene). According to Oostingh, the Cheribonian is the lower of three stages forming together the Pliocene. (Plaisancien, post-Pontien).

Type locality: Cijurei, near Cirebon, W Java.

Geographical distribution: Cipajar Beds in Bantam, Cheribon Beds from Krawang to Semarang, along N Coast of Java; Waled Beds.

Diagnostic fossils. Especially; Turritella angulata acuticarinata Martin. Cited further from Cipacar Beds: Thais, martini Oostingh; Ancilla gerthi Oostingh; Clavus dammermanni Oostingh.

References: Oostingh (C.H.) (1935), p. 227; Oostingh (C.H.) (1938), pp. 508-516; Bemmelen (R.W. van) (1949a), p. 82.

Ludwig (O.) (1933). Toelichting bij blad 30 (Poerwakarta), Geol. Kaart van Java, 1 / 100,000, pp. 13-17.

These beds overlie conformably the Annulatus formation, but the facies changes rather rapidly. In the S of sheet 30 (Jampanmanggun Hills), the following succession was observed: the lowest observable beds are clays with intercalations of andesitic sandstones and fine agglomerates. Then follow volcanics: fine tuffs, coarse agglomerates and andesitic conglomerates and breccias. On top of these are andesitic sandstones and rare marly limestone intercalations, alternating with beds of clay and marl. The top is formed by coarse andesite breccias and agglomerates. An intercalated clay with marine gastropods (Turritella jenkinsi Cossmann) indicates that the volcanics were deposited in marine surroundings.

In the SE of sheet 30, sections in the Cibingbin and Cisaraj Rivers show the following succession:

At the base are clays with intercalations of hard marly limestone.

Then follows a complex of numerous thin beds of andesitic sandstones alternating with clay and shale. A 2-3 m thick limestone was found intercalated in the Cibingbin section, containing corals, echinoids and Operculinella. The top is again formed by a volcanic complex of andesites and andesitic tuff-breccias and sandstones.

In the southern depression of the Tegalwaru Hills are found clay and marls with rare intercalations of sandstone and limestone.

In the northen part of the Tegalwaru Hills the following succession was observed

At the base alternating beds of clay and andesitic sandstone, usually soft and badly exposed.

A middle part of sandstones and dolomitic limestones, all with glauconite. The sandstones are thinly bedded, and contain much clay. Traces of coals are sometimes found, as well as fossil resin. The upper part is formed by a clay with limonitic concretions. In this, most northern occurrence of the Cidadap Beds molluscs were found, though the author does not indicate from which horizon. The molluscs point to an Upper Miocene age (cf. Upper Halang or Cilanang formations). The thickness may reach 1,200 m (in sheet 24) to 2,500 m (in sheet 30).

Type locality: No type locality is indicated. The beds are called after the occurrence in the Cidadap River, long. 107° 13' 27" (= 0° 25' E of Jakarta), lat. 6° 39' S.

Geographical distribution: Sheets 30 and 24 (Bogor) of Geol. Map. of Java, 1 / 100,000. In sheet 30 the beds are mainly found in the Tegalwaru Hills, an anticline striking WNW - ESE, on the N slope over an area, of 30 km long and 9 km broad, on the S slope 30 km long and 3 km broad, further in the extreme SE corner of sheet 30, and along the SW and S parts of the same sheet.

Diagnostic fossils: Rostellaria verbeeki Martin; Paphia neglecta Martin; Ciiltellus dilatatus Martin.

Reference: Bemmelen (R.W. van) (1949), p. 649.

Martin (K.) (1912). Vorlaufiger Bericht ueber geologische Forschungen auf Java, Samml. geol. Reichsmus. Leiden, ser. 1, Bd. 9, pt. 2 p. 171.

Insufficiently defined fossiliferous beds with rich molluscan fauna containing 56 % of recent forms, indicating a Pliocene age.

Type locality: Ci Jajar (Jajar River), near Cirebon (Cheribon) N coast Central Java.

Geographical distribution: Not established.

Reference: van der Meer Mohr (J.C.) (1923), pp. 124-125.

Koolhoven (W.C.B.) (1933). Toelichting bij blad 14 (Bajah). Geol. kaart van Java 1 / 100,000, Dietist Mijnb. Ned. Indie, Bandung, pp. 21-24.

Koolhoven distinguished a Lower and an Upper division. The Lower Cijengkol Layers (member) consist of conglomerates of Old-Andesites and granite, tuffs, breccias, etc., with coal lenses, passing upward into sandy marls with foraminifera. Thickness varying between 200 and 600 m. They pass upwards into the Upper Cijengkol Layers (member) reef-and marly limestones and marls, clay shales and sandstones. Locally they change into sandy marls. Thickness 350 m. In the Eastern part of the Bajar Mountains, the Upper Cijengkol Layers are found lying on top of the Eocene.This points to a progressively overlapping position of the Oligocene deposits (van Bemmelen, 1949a, p. 628).

They are conformably overlain by the Citarate Beds (formation) of Aquitanian age. (A reinterpetation of the Citarate faunas listed here suggests a lower T.e, Late Oligocene age)

Type locality: Cijengkol (village), Bayah Mountains, Residency of Bantam, West Java, 106° 21 '27" E (0° 27' W of Jakarta) 6° 54'25" S.

Geographical distribution: Bayah Mountains, West Java, in the cores of numerous anticlines.

Diagnostic fossils: Lower Cijengkol: Cycloclypeus koolhoveni Tan, Upper Cijengkol: C. oppenoorthi Tan, Lepidocyclina cf. isolepidinoides, Miogypsinoides (Miogypsinella), Nummulites fichteli-intermedius

References: Koolhoven (W.C.B.) (1936), pp. 161-164; Bemmelen (R.W. van) (1949a), pp. 104, 628.

Hetzel (W.H.) (1935). Toelichting bij Blad 54 (Madjenang), Geol. Kaart van Java 1 / 100,000, pp. 32-38.

The above-mentioned author has not originally separated these beds as a distinct formation, but noncomittingly called them "the Pliocene in the SW of the sheet" (i. e. the sheet Majenang). The name "Cijulang Beds" is first introduced by van Bemmelen (1949).

They are conglomerates, sandstones and tuffs of andesitic composition, deposited by a river or rivers. Intercalations of claystone and clay occur, as well as rare limestone layers. The sediments are composed of erosion products of the Kumbang Beds, which they are apparently - at least in part - disconformably overlying, although in the visible contacts there is perfect conformity. Probably the Cijulang Beds are the equivalent of the Tapak, Kalibiuk and Kali Glagah Beds (Formations), although separate units cannot be distinguished.

The Cijulang Beds have typically been deposited near a coastline where positive and negative movements of the sea-level occurred frequently, in fact, exactly as in the above mentioned Pliocene deposits of the Bantarsari and Kaliglagah Basins.

About 100-105 m above the base, vertebrate remains have been found in tuffaceous conglomerates and pebble-beds, alternating, with sandstones. Among these is a Merycopotamus nanus Lydekker, indicating about Middle Pliocene age. This lower part of the Cijulang Beds could therefore be correlated with the Tapak beds more to the East, which moreover occupy a similar position on top of the Kumbang Beds. Elsewhere, especially along the river Cinhonje, marine sandstones occur which contain rich mollusca, faunae, resembling those of the Kalibiuk and Kaliglagah Beds. The total thickness of the beds is 900 m, or more. It must be added that in the upper 400 m local developments of lignite have been found.

Type locality: No definite type-locality can be appointed. The beds are exposed along the Cijulang, a relatively large river flowing in a N-S direction 24 km W of Majenang, forming the border between the provinces W and Central Java. The facies changes rapidly, and no typical section is mentioned. The vertebrate-beds occur near the village Cikadu, long. 108° 32' 17" E. 7° 11' S. Mollusca have been found especially along the Cihonje, a western tributary joining the Cijulang 11.5 km S of the vertebrate locality.

Geographical distribulion: Basin of the Cijulang, between lat. 7° 20' S and 7° 10' 30" S, and a strip 4 km broad between this river. and the town of Majenang, totaling about 125 sq. km.

Diagnostic fossils: Merycopotamus nanus Lydekker, Hexaprotodon simplex von Koenigswald.

Numerous molluscs have been described by Siemon (1929) and Oostingh (1933) to which publications is referred for extensive lists and discussion.

References: Koenigswald (G.H.R. von) (1 933), pp. 29-31; Siemon (R.) (1929), pp. 52, 56; Oostingh (C.H.) (1933), pp. 212-215; Bemmelen (R.W. van) (1949), p. 654.

See: Kaliwangu Beds (Formation) and Cheribonian.

Martin (K.) ( 1911). Vorlaufiger Bericht ueber geologische Forschungcen auf Java. Erster Teil., Samml. geol. Reichsmus. Leiden, ser. 1, vol. 9, pt.1.

Coralline limestones with Lepidocyclina and Miogypsina but insufficiently defined as to stratigraphical and geological position. Possibly they are identical with the Reef Limestone facies (member) of the Cimandiri complex. The author assumed a Burdigalian age, but if they are identical with the reef-limestones, a Vindobonian age must be attributed (Tf 2-4). (Presumed to be a typographic error, although the Lawak beds of central Java are noted by Marks to be Tf3-4. There is no, nor has ever been published, a Tf4. "Vindobonian" is a broad mid and Later Miocene unit that would include Miogypsina in its lowest part.)

The name is obsolete.

Type locality: Ciguha, near Njalindung, W Preanger, W Java,

Geographical distribution: Not established.

Bemmelen (R.W. van) (1949). The Geology of Indonesia, vol IA, p. 651, table 116 on p. 649 fig. 340 on p. 653.

Cross-bedded andesitic and dacitic tuff-sandstones, conglomerates and breccias, to a thickness of 1000 m. The formation contains a Cijulang vertebrate fauna with Merycopotamus nanus Lydekker. It conformably overlies the Kaliwangu Beds and is likewise conformably overlain by the Kaliglagah Beds. The age is therefore approximately Middle Pliocene.

Geographical distribution: Area of about 5 x 3 km on the NW slope of the Cerimai volcano, 30 km WSW of Cheribon (Ceribon); and a second area of 10 x 5 km on the E slope of the same volcano, between Kuningan and Linggajati, 20 kin S of Clheribon (van Bemmelen, 1949, fig. 340).

Martin (K.) (1895). Neues ueber das Tertiaer von Java und die Mesozoische Schichten von Borneo, Samml. Geol. Reichsmus. Leiden, seri, vol. V, pt. 2, p. 42.

Insufficiently defined marine sediments with molluscan fauna containing 51 % recent forms, indicating a Pliocene age (Martin, 1919). Possibly the unit is identical to the Cimanceuri formation. The name is obsolete.

Type locality: Cikeusik, South Bantani, West Java.

Geographical distribution: Not established.

Reference: Martin (K.) (1 919), pp. 121-122.

Martin (K.) (1911). Vorlaufiger Bericht ueber geologische Forschungen auf Java. Erstei- Teil., Samml. geol. Reichsmus, Leiden, vol IX, pt. 1, p. 44.

Marine clays and marls, very fossiliferous, containing a fauna of 189 molluscan species, 33 % of which are recent. Martin concluded from this a younger Miocene age.

Vredenburg considered the fauna as being of Vindobonian age (broadly middle and late Miocene) coresponding approximately to the freshwater Lower Manchar of Nahan of NW India, while the equivalent in Burma is not recognized, or perhaps partly represented by the Akautung Series. (Vredenburg, 1921, p. 328).

Van der Vlerk studied the foraminiferal fauna, corroborating the Vindobonian age (Tf 3) (van der Vlerk, 1924, pp. 17-22).

Gerth has studied the coral fauna (Gerth, 1921, p. 389).

The Cilanang fauna is closely related to the Njalindung fauna but shows a larger percentage of living forms (33 %, in comparison to 18 % and is generally considered to be somewhat younger. The Geological Survey unites the Cilanang and the Njalindung formations in a Middle Miocene stage called the Preanguerian (see Oostingh's Molluscan stratigraphy of the Neogene). They have 91 species in common.

Type locality: Cilanang (Lanang River) W Preanger W. Java. The location is marked as a fossil site on the map of Verbeek & Fenema (1896) on the Lanang River at about 107.3215 deg E, -7.0064 deg S, about 3 to 4 kms NE of the village of Gunung Halu. A further 3 kms NE is the site on the Burial (Boerial) river, at about 107.3495 deg E, -7.0012 deg S.

Geographical distribution: Insufficiently establised, probably West Java only.

Diagnostic fossils: Turritella angulata angulata. Vicarya verneuiili callosa (Jenkins); Siphocypraea caput-viperae murisimilis Martin, L. (trybliolepidina rutteni van der Vlerk.

References. Martin (K.) (1928), pp. 112-118; Vredenburg (E.) (1921), p. 328 Vlerk (I.M. van der) (1924), pp. 16 ff; Gerth (1921), p. 389, Oostingh (C.H.) (1938), pp. 508-526, table; Leupold (W.) and Vlerk (I.M. van der) (1931), p. 639; Bemmelen (R.W. van) (1949), pp. 81-82.

Anonymous (1938), Jaarb. Mijnw. Ned. Indie, Alg. ged., p. 18.

These beds are equivalent to the Cimanceuri Beds on sheet 14 (Bayah) of the geol. map of Java, 1/100,000 and occur in sheets 13 (Rangkasbitung) and 18 (Bogor) of the same map.

The reference given above is only from a preliminary summary of the stratigraphy in the latter sheets, therefore the data are still brief and insufficient.

The formation consists of acid pumiccous tuffs with lense-shaped intercalations of marine sediments with molluscs. In the Southern parts 4 stages may be discerned. At the base 50 m of pumiceous tuffs, then follow 100 metres various tuffs; tuffs with a high content of hornblende: 60 m; some tens of metres various tuffs of indifferent composition, thickness not indicated.

They occur mainly in the Cikeujeup area around Sampangpeundeuj, westwards to Cileles and N to Kaduranca, in the Pasirmuntang area, along the Cimarga River and on both sides of the Cisemeut River from the confluence with the Ciminjak River till past Rankasbitung (All to the West of Bogor, in Bantam, W. Java).

The beds are disconformably overlain by the Bojong Beds.

Type locality: Not mentioned.

Geographical distribution: See above.

Diagnostic fossils: (Op. cit., p. 29), Terebra insulindae P.J. Fisher T. verbeeki Oostingh, Conus sondeianus Martin.

Anonymous (1939). Jaarboek Mijnw. Ned. Indie, (1940), pp. 16-27.

These beds can be divided into two members:

a) One member consists of breccias, sandstones and graywackes, its components are fragments of schists, quartz, mica, tourmaline and volcanics, such as basalt, trachyte, andesite, plagiociase, augite. The former are detritus from pre-Tertiary formations, while the latter may be products from contemporaneous volcanism (van Bemmelen, 1949, p. 618).

b) The other member consists of quartz sandstones and conglomerates, and mudstones. Plant remains and thin coalbeds are intercalated. The facies may be compared to the Bayah Coal Beds also of Eocene age, and situated quite close to the outcrops of the Ciletuh formation. Group (b) may be younger than group (a), but the relation is not yet known.

The thickness of the Ciletuh beds may be 1500 m or more. They are strongly folded and in part metamorphosed into quartzites and graywackes. They are disconformably overlying Pre-Tertiary schists and metamorphic basic rocks (gabbro, peridotite, serpentine) and are in turn discordantly overlain by the Miocene Jampang Series (formation) .

Type locality: Sea coast along Ciletuh Bay, W Coast of the Jampang district, Southern part of Priangan (Preanger), W Java.

Geographical distribution: Area of 20 km by 15 km forming the Western spur of the Jampang region, projecting into the Pelabuban Ratu Bay.

Diagnostic fossils: Nummulites sp., Discocyclina sp., Assilina sp., Pellatispira sp.

References: Pannekoek (A.J.) (1946), pp. 340-367; Bemmelen (R.W. van) (1949a), p. 618.

Duyfjes (J.) (1939). Jaarb. Mijnw. Ned. lndie, (1940), pp. 16-27.

Marine sediments developed in different facies, overlying the Upper Jampang Series and in part overlain by young Neogene volcanic effusiva. The following lithologic facies may be distinguished:

1. The Lengkong beds (formation): marls, mudstones and calcareous sandstones with hard platy limestones in the higher part of the section; tuffaceous matter is a minor constituent. They occur in an isolated syncline N of Lengkong (see geographic distribution).

2. The Reef-Limestones (formation): a 250-300 m thick complex of unstratified, hard coral limestones and soft, porous Globigerina limestones, passing Eastward into platy limestones. Found near Bojonglopang.

The Lengkong Beds (formation) and the Reef-Limestones formation are names introduced for what was originally known as the Annulatus Formation, a name which is not sustainable because of the fact that C. annulatus occurs down to the Lower Miocene of the Jampang sedimentary series.

3. The Nyalindung Beds (formation): mudstones, sandy clays and claystones, glauconitic sandstones and conglomerates. They are rich in marine molluscs and corals, but also lignite seams and combustible shales are found in this series.

Near Bojonglopang the Nyalindung formation lies on top of the reef limestones formation, but elsewhere it forms lenticular intercalations in the latter, so that these formations may be assumed to be contemporaneous.

The included foraminiferal fauna indicates a Middle Miocene age (Vindobonian) (Tf2-3).

Type locality: Valley of the Cimandiri (Mandiri river) Jampang district, Southern part of West Java.

Geographical distribution: Jampang district.

Diagnostic fossils: Miogypsina indonesiensis Tan, M. bifida Rutten M. polymorpha Rutten; Cycloclypeus annulatus Martin Turritella angulara angulata Martin.

Reference: Bemmelen (R.W. van) (1949a), pp. 81, 620.

Koolhoven (W.C.B.) (1933). Toelichting bij Blad 14 (Bajah). Geol. Kaart van Java 1: 100,000. Dienst Mijnb. Ned. Indie, Bandung, pp. 32-37.

Fossiliferous marine sediments, consisting of soft, tuffaccous, polymict calcareous conglomerates and sandstones, dacitic tuffs, hard shell-breccias, etc. In the clastic sediments, debris of the Old Andesite Formation is found, as well as quartz and quartz-sandstone from the Eocene formations. The matrix is usually calcareous, sometimes tuffaceous, sometimes also glauconitic.

The tuffs consist of dacitic ashes with quartz, acid plagioclase, biotite and hornblende.

Towards the north the sediments become increasingly volcanic non-marine, and consist of coarse polymict conglomerates, breccias and tuffs, with much silicified wood. The breccias and tuffs are here mainly andesitic, though dacite occurs.

The formation contains a rich molluscan fauna, part of which was already determined by Martin (1899, 1919). Oostingh eventually determined 117 species, 48 % of which are recent. Miocene larger foraminifera are absent, from which a Lower Pliocene age was concluded. The thickness of the formation is about 250 m.

The formation disconformably overlies Eocene, Oligocene and Miocene formations. It occurs, however, mainly in fault-basins, and the superposition is not everywhere clear. The formation is overlain by Holocene deposits.

Type locality: Cimanceuri River, between 3.5 to 1.5 km NNW of Bayah, long. 106° 15' 7" E (0° 33' 20" W of Jakarta), lat. 6° 54' 30" S.

Geographical distribution: Mainly in an area of about 8 x 7 km. W and N of the type locality, bordered by faults (graben), and in numerous smaller fault basins to the West, also on sheet 10 (Malingping).

Diagnostic fossils: See text.

Reference: Bemmelen (R.W. van) (1949a), p. 630.

Koolhoven (W.C.B.) (1933). Toelichting Blad 14 (Bajah). Geol. Kaart van Java, 1: 100,000. Dienst Mijnb. Ned. Indie, pp. 27-29.

The Cimapag beds consist of a mixture of marine and volcanic facies. The volcanic facies consists of andesitic and dacitic tuffs and agglomerates, intermingled with detrital products of older formations, such as boulder and pebbles of limestone, marl, mudstone, quartz sandstone, conglomerate, chert, etc. The marine facies consists of sandstones, clays and occasional reef-limestones with larger foraminifera, indicating an Aquitanian to lower Burdigalian Age (Te5).

The Cimapag Beds discordantly overlie all older, Oligocene, Eocene and Lower Miocene Beds. They are disconformably overlain by the Sareweh Beds (formation) of Burdigalian age.

Type locality: Cimapag (Mapag River), Bayah Mnts, Residency of Bantam, Western Java.

Geographical distribution: Marginal belt around the central Bayah Mountains.

Diagnostic fossils: Lepidocyclina (Nephrolepidina) inflata Provale; L. (N.) ferreroi Provale; Spiroclypeus leupoldi v. d. Vlerk; S. cf tidunganensis v. d. Vlerk; Miogypsina dehaarti v. d. Vlerk; M. thecidaeformis Rutten; Trillina howchini (Schlumberger).

Reference: Bemmelen (R.W. van) (1949a), p. 629.

Martin (K.) (1895). Neues uber das Tertiar von Java und die mesozoische Schichten von W Borneo. Samml. d. geol. Reichsmus, Leiden, ser. 1,. vol. 5, p. 45.

Fossiliferous marls with marine littoral facies and tuff-sandstones, partly overlying the reef-limestones formation of the Cimandiri, partly supposed to pass laterally into the Nyalindung formation of the Cimandiri group. They contain a rich molluscan fauna studied by Martin (1919). 42 % of this fauna is still living, from which an Upper Miocene age was determined. Moreover they contain Turritella angulata cramatensis, which, according to Oostingh, places the layers in the same stratigraphical position as the Genteng- and the Cimandiri formation of his stratigraphy (Ciodeng stage; not the same as the Cimandiri group).

Vredenburg (1921) considered them as Pontian in age, about equivalent to the Akautaung series and the lower part of the freshwater Irrawaddy series of Burma, the marine Talar stage of the Mekran Series, and the Middle Siwalik of NW India.

According to van Bemmelen (1949), the Ciodeng formation may possib1y be divided into an upper and a lower part, the former equivalent to the Naylindung formation of the Cimandiri group, and an upper part (Ciodeng formation sensu stricto) which may be correlated with the upper Miocene Beser beds (formation).

Type locality: Ciodeng, N of Cimandiri, West Java.

Geographical Distribution: Between Pelabuhan Ratu and Cibadak, Preanger, Western Java.

Diagnostic fossils: Turritella t angulata cramatensis Martin.

Reference: Martin (K.) (1928), pp. 118: Martin (K.) (1900), p. 160 Vredenburg (E.) (1921), p. 328; Oostingh (C.H.) (1938), pp. 508-526 Bemmelen (R.W. van) (1949), pp. 82, 620.

See: Oostingh's Molluscan Stratigraphy Of Neogene.

Anonymous (1938). Jaarb. Mijnvt,., Alg. ged., p. 18.

The above reference is of a preliminary summary on the stratigraphy of sheets 13 (Rankasbitung) and 24 (Buitenzorg) of the geol. map of Java 1: 100,000. The data are therefore of necessity brief and insufficient, no type locality or geographical distribution can be given. Overlying the Genteng Beds with an indistinct unconformity, are 400 m of pumiceous tuffs (sometimes pisolithic (?)), passing upwards into tuffaceous, glauconiferous marls with marine molluscs, clays and sandstones with local intercalation of andesitic breccias. Fossil wood is scarce. These beds are reported from several localities:

1. Along the river Cisemeut, in a strip 5-6 km broad between Leuwidamar to the line Sinupati-Lebakwaru-Munjol.

2. A 3 km broad strip from Dalung-Cisolear to the road near Pr. Cidadap.

3. A small area 1 km NW of Sampangpeundeuj; all in Bantam, W. of Bogor, West Java.

Diagnostic fossils: (op cit., p. 29): Turritella angulata acuticarinata Dkr.; Thais martini Oostingh; Ancilla gerthi Oostingh.

These fossils belong to Oostingh's Cheribonian (Lower Pliocene) stage.

Bemmelen (R.W. van) (1941). Toelichting bij Bladen 73 (Semarang) en 74 (Oengaran). Geol. Kaart van Java, 1: 100,000, pp. 29-3 1.

The Cipluk Beds conformably overlie the Banyak Beds. They consist of white to greenish, tuffaceous Globigerina-marls, alternating with tuff sandstones. Larger foraminifera have never been encountered. In the SE of sheet 74 the beds contain quartz and other fragments, indicating erosion of pre-Tertiary beds. The thickness is unknown, but is at least a few hundreds metres.

On the upper side the Cipluk Beds are typically limited by a limestone zone (Kapung limestone member) which occurs exclusively along the N. side of the N. Serayu Mnts. The limestone is very variable in thickness, and is sometimes completely absent. The maximal thickness is about 100 m in the W and 150 in the East of the sheets. Very rare Lepidocyclina have been encountered, so that the age is probably still uppermost Miocene. In the original paper van Bemmelen assigned a Lower Pliocene age to the beds; in 1949, however, an uppermost Miocene age was assumed to be more probable, because of the rare occurrence of Trybliolepidina in the Kapung Limestones. The limestones are conformably overlain by the Kalibiuk Beds.

Type locality: Cipluk, sheet 74, geol. map of Java 1 / 100,000.

Geographical distribution: Near Kaloran, in the area between the rivers K. Bade and K. Tuntang, along the N. rim of the N. Serayu Mnts.

Reference: Bemmelen (R.W. van) (1949), pp. 606, 573.

See: Halang Beds.

Ludwig (O.) (1933). Toelichting bij Blad 30 (Poerwakarta). Geol Kaart van Java, 1: 100,000, p. 18.

These beds overlie transgressively the Cidadap Beds, with a basal conglomerate consisting mainly of andesitic-basaltic elements. The upper part of the beds is formed by marly tuffs with intercalations of tuffaceous sandstones and breccias. No fossils have been found. The position of the beds indicates that they are probably equivalent to the Kaliwangu / Cijurei Beds, of Pliocene age.

Type locality: Citalang, at tributary of the Ciherang, near the E limit of sheet 30, East of Purwakarta.

Geographical distribution: Near type locality only. See Kaliwaligu and Cidiurei Beds (formation).

Diagnostic fossils: None.

Reference: None.

Koolhoven (W.C.B.) (1933). Toelichting bij Blad 14 (Bajah). Geol. Kaart van Java, 1: 100,000. Dienst. Mijnb. Ned. Indie, pp. 24-27.

At the base the formation consists of reef-limestones, while the upper part forms a complex group of rocks called "Tuffite zone". The limestone contains terrigenous detritus, like quartz, plagioclase, and shale fragments. The tuffite zone comprises tuffaceous limestone-gravels, conglomerates, breccias, sandstones, marls and limestones, always with clastic matter, particularly derived from the Old Andesite Formation. The thickness is 1200-1500 m.

In the South of' the Bayah Mountains the Citarate Beds overlie conformably the Upper Cijengkol Beds (formation). They are unconformably overlain by the Cimapag Beds formation. The fauna points to an Aquitanian age (Te1-4).

Type locality: Citarate village, Bayah Mountains, Residency of Bantam, West Java, long. 106° 22' 27" E (0° 26' W of Jakarta), lat. 6° 56' 13" S.

Geographical distribution: Southern part of the Bayah Mnts, in numerous small, scattered outcrops, owing to intricate blockfaulting.

Diagnostic fossils: Cycloclypeus ex gr. eidae Tan; Lepidocyclina (Nephrolepidina) cf. sumatrensis var. minor Rutten; L. (Nephrolepidina) isolepidinoides v. d. Vlerk; Eulepidina cf. formosa (Schlumberger); Spiroclypeus tidunganensis v. d. Vlerk; S. margaritatus Schlumberger; S. leupoldi v. d. Vlerk; Miogypsina bantamensis Tan (Miogypsinella ?); Trillina howchini (Schlumberger) (All Austrotrillina species in modern usage).

References: Koolhoven (W.C.B.) (1936), pp. 161-164; Bemmelen (R.W. van) (1949), pp. 628-629.

Bemmelen (R.W. van) (1949). Geology of Indonesia,, vol. 1 A, p. 639.

Mainly andesitic tuffs, conglomerates and sandstones deposited in marine surroundings, with lenses and intercalations of marine limestones and clay shales. A lower and an upper series may be distinguished separated by a dacitic pumice breccia. The total thickness of the formation is 3,400 m. The marine intercalations contain larger foraminifera. The beds overlie the Lower Miocene Masigit (= Rajamandala) limestone formation and are overlain by the upper Middle Miocene Cimandiri Complex (group), with the Cilanang Fanuna of Oostingh (Preanguerian). The age of the Citarum Beds must therefore be lower Middle Miocene.

Type locality: Valley of Citarum River, West of Cianjur, near Bandung, West Java.

Geographical distribution: Rajamandala anticline, between Cianjur and Padalarang, near Bandung, West Java.

Diagnostic fossils: Miogypsina thecidaeformis Rutten; Lepidocyclina cf. angulosa Provale; Eulepidina sp., Cycloclypeus sp.

Anonymous (1928). Jaarb. Mijnb. Ned. Indie, alg. ged., pp. 72-73.

Well bedded andesitic-trachytic conglomerates, sandstones, quartz-sandstones, marls, clays and foraminiferal limestones. According to Koolhoven (1933) the Citarucup Layers overlie the Lower Eocene Bayah Layers (formation) and are unconformably overlain by Lower Oligocene Lower Cijengkol Layers (formation).

According to Leupold and van der Vlerk (1931) the foraminifera in the layers are strongly resemblant to those of the upper Nangulan Eocene Series.

See remarks from B.P.M. at Jiwo layers.

Type locality: Citarucup (village), Bayah district, Bantam, W Java, long. 106° 21' 12" E (0° 27' 15" W Jakarta), lat. 6° 49'29" S.

Geographical distribution: Bayah Mountains, Residency of Bantam, West Java, on sheet 14 in an area of 4 x 4 km around type locality

Further in an anticlinorium E of Bayah village over a surface of 10 x 8 km in numerous anticlinal cores to the W, probably continuity on sheet no 10 (Malingping) (unpublished).

Diagnostic fossils: Discocyclina dispansa Sowerby var. minor Rutten Discocyclina pengaronensis (Verbeek) Pellatispira; Nummulites vredenburgi Provale; N. djogjakartae (Martin).

References: Leupold (W.) and Vlerk (I.M. van der) (1931), p. 634; Koolhoven (W.C.B.) (1933), pp. 20-21. Koolhoven (W.C.B.) (1936), pp. 161-164; Bemmelen (R.W. van) (1949), pp. 104, 628.

Bemmelen (R.W. van) (1949). The Geology of Indonesia, vol. IA, pp. 60-6 1.

"Crystalline schists are widely distributed in the Indian Archipelago, but there is much diversity of opinion as to their age. The crystalline schists certainly do not belong to a distinct geological epoch, neither are they of an archaic age as has been supposed by many earlier authors. Sedimentary deposits of various ages can be altered into crystalline schists, by regional metamorphism, aided by contingent processes of solid diffusion of constituents. Often a succession of alterations can be distinguished under the microscope, giving them a polymetamorphic appearance and enabling us to distinguish between several types of schists (viz. crystalline schists and phyllites).

"In some areas the transition of fossil-bearing strata made possible a direct age determination, while in other areas only the upper limit is fixed by the age of the first transgressive formation. Here under some instances are mentioned

* Sumatra: The crystalline schists of S Sumatra (Geol. map Sum., 1/200,000, 1, 2, 4, 5) North Sumatra (van Bemmelen, 1932a) are presumably parts of an old Basement complex of pre-Mesozoic age. Mesozoic sediments of Sumatra in many localities show a phyllitic facies.

* The schistose and phyllitic formations of the smaller islands on the Sunda Shelf are generally of young Paleozoic and Upper Triassic age (van Bemmelen, 1940).

* Crystalline schists of West and Central Borneo are older than Upper Triassic (Z. v. Emmichoven, 1939) and partly also older than the Permo-Carboniferous (Zeylmans v. E., 1939, pp. 56-58); but also younger formations may have a schistose facies, e.g. the Eocene has obtained in some belts a phyllitic character (ter Bruggen, 1935). Zeylmans v. E. published in 1940 a study, in which he described the schists and gneisses from the Schwaner Mnts in Central Borneo, which are considered to be older than the Permo-Carboniferous. The crystalline schists of the Meratus Mnts in SE Borneo are older than the Alino Formation (? Jurassic, ace. to Koolhoven) which contain detrital material of the schists.

* The polymetamorphic crystalline schists of Celebes are older than the Mesozoic or Young Palaeozoic (Brouwer, 1941, pp. 257, 258) but there are also phyllites of Mesozoic and Eocene age (Tinombo Form., Pompangeo Form., Maroro Formation).

Recent contributions to the petrology of the crystalline schists of Central Celebes were made by Willems (1937), Egeler (1946, 1948) and de Roever (1947).

* In SE Celebes and Buton, Bothe (1927) distinguishes a metamorphic (phyllitic facies) of the Mesozoic (Kendari Facies) from a less or non-metamorphic facies (Buton Facies).

* In the Northern Moluccas isolated outcrops of crystalline schists are found on Obi (Brouwer, 1923, p. 47) and on Bacan (Sibella Mnts), which might be metamorphic Paleozoic rocks, while in the Sula Islands (Brouwer, 1920, 1925) their age could be fixed as pre-Liassic.

* In the outer arc of the Southern Moluccas crystalline schists are widely exposed. In Seram distinction can be made between phyllites which are pre-Upper Triassic (Presumably young Palaeozoic) and older polymetamorphic crystalline schists (Valk, 1945; Germerad, 1946).

* In Leti transition from epimetamorphic schists to phyllitic rocks with intercalations of Permian crinoidal limestones are found (Molengraaff, 1915).

* In Timor crystalline schists occur in an overthrust complex of rocks, associated with ophiolites. These schists are at least pre-young Mesozoic, and partly pre-Permian (Brouwer, 1942).

* In the islands West of Sumatra exposures of schistose pre-Tertiary rocks are known. Terpstra (1932) mentions phyllites and amphibolites from Sipura and at the west coast of Nias crystalline schists crop out at the base of the Palaeogene near Sumasuma.

The oldest pre-upper Palaeozoic and presumably more or less autochthonous outcrops of crystalline schist are found in Central Sundaland (West and Central Borneo and the Lampongs district in S Sumatra). The crystalline schists in the circum Sunda System form parts of overthrust complexes and are partly pre-young Palaeozoic, partly young Palaeozoic, Mesozoic and even Eocene."