Definitions of Pre-Pleistocene formation names in Java

Pleistocene formations are in a separate file

INDEX

Sambupitu Layers, Sareweh Beds, Second Breccia Horizon, Second Marl-Tuff Horizon, Selorejo sand Member, Semilir Beds, Sentolo Beds, Sigugur limestone, Sonde Beds, Sondien Stage, Southern Mountains Miocene, South Serayu Miocene, Tagogapu limestone, Tapak Beds, Tawun Fm., Third Breccia Horizon, Third Marl Tuff Horizon, Tuban Fm., Untere wirbeltierhorizont, Waled Beds, West Progo Beds, Wonocolo Fm., Wonosari limestone, Wungkal Layers

See: Southern Mountain Miocene

Koolhoven (W.C.B.) )1933). Toelichting bij blad 14 (Bajah). Geol. kaart van Java 1 / 100,000, Dienst Mijnb. Ned. Indie.

Reef limestones, marls, sandstones and tuffs to an aggregate thickness of about 1 000 m. To the E the limestones disappear and are replaced by clay.

The basal strata of the Sareweh formation still contain tuff-beds belonging to the volcanic stage of the preceding Cimapag Beds (Formation), which they overlie with a slight stratigraphical hiatus. They are overlain by the Badui Beds (Formation), in the NW disconformably, but this disconformity disappears eastward.

The contained fauna indicates a Lower Burdigalian age (Te 5); in fact the fauna does not differ much from that of the underlying beds, except for the presence of Flosculinella.

Van Es correlated these beds with the Gumai Formation (= Telisa Formation) of S Sumatra.

Type locality: Sareweh village, Bayah Mountains, Badui district Residency of Bantam, West Java, 106° 11' 20" E, 6° 39 '45" S (SW corner of sheet 13).

Geographical distribution: Not yet well established: to the NW of the Bayah Mountains in the NW corner of sheet 14, in a strip 15 km in EW direction, about 1,5 km broad, forming the core of an EW striking anticline.

Diagnostic fossils: Lepidocyclina (Nephrolepidina) ferreroi Provale, Miogypsina polymorpha Rutten; Austrotrillina spp. [=Trillina howchini] (Schlumberger), Flosculinella globulosa (Martin).

References: Bemmelen (R.W. van) (1949a), p. 629; Bemmelen (R.W. van) (1949b), pp. 14-15.

See: Southern Mountain Miocene

See: West Progo Beds

See: Merawu Beds. Sigugur Limestone Member.

Martin (K.) (1895). Neues ueber das Tertiaer von Java und die mesozoischen Schichten von West Borneo. Samml. Geol. Reichsmus. Leiden, Ser. 1, vol. V, p. 36.

Marly facies of the Upper Kalibeng Beds. The marls are only locally developed, and laterally pass into a limestone facies, the Klitik limestone member.

The beds overlie the Lower Kalibeng formation, and are overlain by the Pleistocene Pucangan formation. They contain a fauna which according to Martin (1919) contains 53 % of recent forms, indicating an Upper Pliocene Age. Deposits of the same age occur near Padasmalang and Pengkol, near Sonde, and Sangiran, N of Surakarta.

Vredenburg (1921) regarded the Sonde-beds as equivalent to the fresh-water Irrawadi formation of Burma, and to the marine Gwadar Stage, the Upper Manchar and the Upper Siwalik of NW India.

The marls contain a rich molluscan fauna, which Oostingh (1938) has included in his Sondian molluscan stage of the Tertiary of Java. The age of this stage lies in between Cheribonian stage below, and the Bantamian stage above.

Type locality: Sonde, near Trinil, district of Ngawi, Solo river valley, East Java.

Geological distribution: Northern part of East Java, Kendeng Hills.

Diagnostic fossils Turritella angulata tjicumpeiensis (Oosting); Terebra verbeeki Martin T. insulinidae; Conus sondeianus Martin.

References: Martin (K.) (1900a), pp. 3, 4; Martin (K.) (191la),p. 194 Martin (K.) (1919), pp. 29, 141-143; Vredenburg (E.) (1921), p. 328 Oostingh (C.H.) (1938b), pp. 508-526; Es (L.J.C. van) (1931), p. 122, table; Bemmelen (R.W. van) (1949a), pp. 82, 573.

See: Oostingih's Molluscan Stratigraphy of the Neogene.

Bothe (A.Ch.D.) (1929). Djiwo Hills and Southern Range. Excursion guide Cl, 4th Pacific Science Congress, Java.

A series of mixed volcanic and flysch-like marine deposits, forming the Southern Mountains (Gunung Kidul) of Central Java, with a total thickness of about 4,500 m.

The series unconformably overlies folded Pre-Tertiary and Eocene (Jiwo Layers), and may be subdivided into the following stages (from above downward):

Kepek layers (Formation) (Kepek lagen): Marls and limestones, with Globigerina and Lepidocyclina flexuosa as well as the mollusc Vicarya callosa, indicating a Vindobonian (Preanguerian) age, Tf3. Thickness in the Wonosari-Baturetno basins: 200 m. Laterally the marly facies passes into the reef-limestone facies of the upper part of the next stage

Wonosari Limestones (Formation): Bedded limestone with locally numerous bioherms of Hexacorals, attaining a thickness of about 800 m between Pacitan and Wonosari. The Wonosari limestones contain the larger foraminifera Lepidocyclina sp., Miogypsina polymorpha Rutten, M. thecidaeformis Rutten and near Pacitan: Flosculinella globulosa and F. bontangensis (Te5-fl). Van Bemmelen correlates these beds with the Sentolo Beds of the West Progo Mnts. If this may be partly true, the lower part of the Wonosari limestones, i. e. the outcrops near Pacitan in the Thousand Mountains (Gunung Sewu), contain corals which indicate distinct affinity with the Jonggrangan) fauna (Osberger, 1954)

Species with X in front of the name are known from the Jonggrangan (Djungrangan) Beds, with o behind the name were only known from Borneo until recently).

The larger part of the cited specimens are from old Miocene beds. A large number (8) are known from the Jonggrangan (=Djungrangan) Beds, especially the occurrence of the genus Ceratophylliella is, according to Oserberger, typical for the Jonggrangan Beds. Moreover, the Jonggrangan beds are characterized by the same larger Foraminifera, a.o. Flosculinella globulosa and F. bontangensis, indicating a Burdigalian (Te5 - Tf 1) age. Near Pacitan (Punung) the marine limestones laterally pass into a mixed marine-volcanic, eventually an entirely volcanic, facies. This mixed marinevolcanic facies has been given the name of Oyo Beds (Formation) by Bothe (A.Ch.D.), where they occur South of the Jiwo Hills. These Oyo Beds contain Cycloclypeus annulatus and Trybliolepidina rutteni, indicating an upper Burdigalian age (T. f.). Possibly they are the equivalent of the upper Part of the Wonosari limestone, and pass laterally into these.

They consist of about 350 m (i.e. near Jiwo) of andesitic tuffs, tuffaceous marls and clays, limestone breecias and conglomeratic limestones. The limestones contain, apart from the above mentioned larger foraminifera L. (Nephrolepidina) ferreroi Provale; L. inflata Provale; Miogypsina poIymorpha Rutten; M. thecidaeformis Rutten.

The Oyo beds may thus be correlated with the basal conglomeratic layers of the Sentolo Beds farther West, which incidentally are characterized by the same variety of vitreous tuff. According to Van Bemmelen (1949) this tuff is due to the activity of the Banyak volcanoes (See Banyak Beds, Kendeng zone).

The Oyo Beds, like the basal Sentolo Beds, are transgressive over the underlying layers, sometimes with a distinct angular unconformity, e.g. South of Jiwo.

The following formations belong to the Lower Miocene, and are at least for a part equivalent to the lower Wonosari Limestones to the East and to the Jonggrangan beds to the West:

Sambupitu layers (Formation): A thick complex of sandstones and shales of marine origin, with at the base coarse unbedded volcanic agglomerates, distinguished as the Nglarangan layers. Together they are about 1,000 m thick. The marine upper part contains: L. (Nephrolepidina) verbeeki; L. (Nephrolepidina) ferreroi; L. (Nephrolepidina) sumatrensis; Cycloclypeus communis; Miogypsina polymorpha Rutten; M. thecidaeformis Rutten; indicating a Burdigalian age. The Sambupitu-Nglarangan beds overlie the Semilir Beds (Formation): an entirely volcanic series, consisting of white tuffs and shales, dacitic pumice tuffites, dacitic breccias, about 1,000 m thick. They overlie the partly marine Butak Beds (Formation), a flysch-like series of regularly altering shales, sandstones in thin layers and acid tuffs. The sandstones do not contain distinct fossils, but show on their curious worm-like traces, and internal moulds of Cidaris-like echinids.

This monotonous series may be about 1,000 m thick.

They overlie another series of shales sandstones and conglomerates very much the same:

The Kebo Beds (Formation), which overlie possibly directly the pre-Tertiary and Eocene of the Jiwo Hills. In the sandstones, shales and volcanic tuffs and agglomerates we find here intercalated two sills of basaltic andesite. The thickness of these beds, which are less well disclosed, may be about 1,000 m.

Type localities: Kebo Beds: Gunung Kebo (Kebo Mntn), S of Jiwo Regency Klaten, Residency Yogyakarta; Butak Beds: Gunung Butak, idem Semilir Beds: Gunung Semilir, idem; Nglangran Beds: Bukit Nglangran, idem; Sambupitu Beds: Sambupitu, idem; Oyo Beds: Kali Oyo, idem (Ojo River); Wonosari Limestones: Wonosari (small town), Southern Mountains Kepek Beds: Kali Kepek (Kepek river) near Wonosari, idem.

Geographical distribution: Southern Mountains (Gunung Kidul), Southern part of Central Java; Gunung Sewu, idem.

Diagnostic fossils: See in text.

References: Bothe (A.Ch.D.) (1929); Bothe (A.Ch.D.) (1934; Bemmelen (R.W. van) (1949a), pp. 108-109, 554-558.

Harloff (Ch.E.A.) (1933). Toelichting bij blad 67 (Banjarnegara). Geol. Kaart van Java 1: 100,000, pp. 20-25.

The Miocene of the South Serayu Mnts has been deposited discordantly on top of the Eocene. It has been subdivided by Harloff into three Tuff marl "Horizons" (formations) and three Breccia "Horizons" (formations).

1. First Marl-tuff Horizon (formation) (Eerste Mergeltuffhorizon). These are the oldest beds disconformably overlying the Eocene. Well-bedded with ash-tuffs, with sponge-spicules, radiolaria, and globigerinids. Intercalated clay lenses, locally developed, contain Miogypsina and Flosculinella globulosa indicating Lower Burdigalian Age (Te5). Thickness varying between 0-300 m.

2. First breccia-horizon (formation) (Eerste Brecciehorizont). Concordantly overlying the First Marl-tuff Horizon. Mainly consisting of sandstones, conglomerates and breccias of andesitic and basaltic eruptiva. The sandstones usually well-bedded, mainly occur at the base of the formation, followed by conglomerates and breccias, at the top again overlain by sandstones. This sucession is not continuous, and lateral facies changes are more or less in evidence in many places. Small limestone lenses indicate a generally marine sedimentation. They contain corals and Lithothamnium, while Lepidocyclina have been encountered. The thickness of this formation is about 1,200 m.

3. Second Marl-Tuff Horizon (formation) (Tweede Mergeltufhorizont). Concordantly overlying the First Breccia Horizon. Consisting of white marly tuffs, much resembling the F.M.H. White glassy tuffs mixed with clay, mixed in different proportions with lime. Larger foraminifera contained: Nephrolepidina inflata; N. ferreroi; Trybliolepidina rutteni; Miogypsina thecidaeformis; Cycloclypetis eidae; C. inornatus; C. indopacificus var.

They indicate an Upper Burdigalian age (Tf 1).

The fossils occur in small lenses throughout the layers. There is one fossil horizon. In the West this horizon is about 15 m above the base of the layers, in the East about 400 m. This probably indicates an increased rate of sedimentation in the central part of the basin only if this correlation runs in the strike of the basin, which probably is the case, the correlation being from West to East.

Farther East the distance between fossil horizon and base is reduced again to 250 m. According to Van Bemmelen (1937, p. 50), the S.M.H. may be correlated with the Lower Penyatan Series.

4. Second Breccia Horizon (formation) (Tweede Brecciehorizont). Discordantly resting on top of the preceding. Strong volcanic activity results in deposition of basaltic lahar breccias, lava flows and dikes of olivine basalt. The thickness of this series is strongly variable.

According to Van Bemmelen (1937) this formation may be correlated with the Middle Penyatan Series.

5. Third Marl Tuff Horizon (formation) (Derde Mergeltufhorizont). Erosion products of the preceding stage. Where the S.B.H. lacks, this horizon is disconformably overlying the S.M.H. A lower part of this horizon consists of marly tuff-sandstones and conglomerates, the sandstone varies from 0 in the East to about 200 m in the Western part of the basin. The second or upper part is about 600 m thick, total thickness about 800 m. According to Van Bemmelen (1937) this horizon may be correlated with the Upper Penyatan Series.

6. Karangbolong Limestone (formation). (Kalksteen van Karangbolong). Coralline limestones in reef-facies with larger foraminifera, o.a. Trybliolepidina rutteni. The limestones rest horizontally on top of folded maris of the T.M.H.

6a. Stratigraphically equivalent to 6, are conglomerates and coarse breccia, named the basal layers of the Third Breccia Horizon. These layers occur in depressions, and are the remnants of the erosion products formed after the orogenic phase at the end of the preceding period.

The layers are strongly variable: sandy loams and clays, with quartz and mica, quartzose gravels, polymict conglomerates containing elements of the pre-Tertiary subsoil. The material came from the North. Like the Karangbolong Limestones, they discordantly overlie the folded T.M.H. Towards the NW these conglomerates pass into clay-marls of Pliocene age.

According to Van Bemmelen (1937) this horizon may be correlated with the Basal Limestone of the Bodas Series.

7. The Third Breccia Horizon, disconformably overlies all preceding, folded, formations. It consists of about 700 m andesitic breccias and agglomerates, unbedded, and without fossils. Its age is assumed to be already Lower Pliocene.

According to Van Bemmelen (1937) this horizon may be correlated with the Bodas series .

Type locality and Geographical distribution. South Serayu Mnts, near Banjarnegara, C. Java.

Diagnostic fossils: see text above.

References: Bemmelen (R.W. van) (1937), p. 50., Bemmelen (R.W. van) (1949a), pp. 602-604.

Haar (C. ter) (1934). Toelichting bij Blad 58 (Boemiajoe). Geol. kaart van Java, 1 / 100,000, pp. 21-27.

The Tapak Beds consist of two parts: a basal coarse clastic and partly volcanic member which passes gradually upwards into an upper limestone member, which, however, seems to be developed only locally (Reef limestones).

A typical section along Cipanas River near Bantarsari shows the following sucession; conformably overlying the Kumbang formation are layers of coarse greenish sandstones and conglomerates, alternating with thin layers of andesitic breccias. Upwards the sandstones grow less and less coarse, the andesitic breccias disappear, as do the conglomerates, while layers of marl begin to be intercalated. The upper part consists of a regular alternation of sandstones and green marls, in which the sandstones are calcareous and contain fragments of marine molluscs. The top of the series is formed by a bed of coralline limestone. The total thickness is about 500 m in sheet 58, diminishing to zero towards the West in sheet 54.

Reef-limestones are developed locally, on other localities the upper part the Tapak formation consists of marls and sandstones. In the Western parts of the occurrence, the limestone-facies is completely lacking. The formation is overlain by the Kalibiuk formation, probably conformably. The beds are very fossiliferous. The coralline limestone contains larger foraminifera, the marls and sandstones mollucs, and the basal beds contain remains of mammals, which have, however, not been determined. It is probable that they may be correlated with the Cijulang Beds (formation) which contain a middle Pliocene mammalian fauna (Tatrot). The mollusca are about 60 % recent forms, indicating a Lower Pliocene age. The molusca (Melania) are partly from brackish water, partly from the tidal zone (Oostingh, 1935, p. 220). The corals offer widely varying percentages of recent forms, and cannot as yet be used for age determination. The larger foraminifera consist of species of Operculina and Cycloclypeus, and indicate a Pliocene age. If the Pliocene is divided into three parts, the Tapak beds may be assumed to occupy the Middle Pliocene, if it divided into two (the official subdivision of the geological survey) the Tapak Beds are tentatively assigned to the lower part (n4 of Tg2).

Type locality: The beds are named for an occurrence near Gunung Tapak, 12 km NNE of Bantarkawung, map sheet 58 of Geol. Survey. As type-locality it is better to assign the section in the Cipanas River, 2 km NW of Bentarsari, long. 109° 18' 30" E, lat. 7° 8' 20" S.

Geographical distribution: along the rim of the Bentarsari Basin, an intra-montane basin of irregular diamond shape included in the Kumbang Mnts, between long. 108° 45' 30" and 108° 53' 30" E. lat 7° 7' 40" S and 7° 10' 50" S. Further S of G. Tapak, NE of Bantarkawung, and in the extreme SW part of sheet 58 and extreme SE part of the adjoining sheet 54 of the geol. survey of Java.

Diagnostic fossils: Cycloclypeus reticulatus Caudri, C. cf. guembelianus Brady: C. postindopacificus var. tenuistriatus Tan; Operculina complanata (Defrance).

Numerous molluscs and corals have been described; for the mollusca

see: Oostingh, 1935, for the corals see Gerth, 193 1, pp. 149-150.

References: Hetzel (W.H,) (1935), pp. 24-27; Gerth (H.) (1931), pp. 149-150; Oostingh (C.H.) (1935); Bemmelen (R.W. van) (1949a), pp. 606, 654.

See: Kaliglagah Beds, Lower Vertebrate Zone.

This is the same (Vertebrate zone) as in the Bumiaju beds.

Here once more called Pliocene (V. Koenigswald).

See: Menenteng Canyon Beds.

Obsolete name.

Martin (K.) (1912). Vorlaufiger Bericht uber geologische Forschungen auf Java. 2 Teil. Samml. geol. Reichsmus. Leiden, serie 1, Bd. 9, pt. 2, pp. 108-200.

The above mentioned author introduced the name "Schichten des West Progo Gebirges" for a series of limestones, marls and reef-limestones outcropping over large surfaces in the hills west of the Progo River, south central Java (these are the first range of hills west of Yogyakarta, about 20kms out of the city and now known as the Menoreh Hills). Among the molluscs collected in these strata he found 8 % of recent forms, indicating an Oligo-Miocene age (Aquitanian-Burdigalian; Aquitanian for the reef-limestones).

Between 1920 and 1940 some more work was done on the West-Progo Mountains (see litt. below): At the base of the Tertiary the Eocene layers of Nanggulan, and overlying these a mainly volcanic facies, the so-called Old Andesites Formation of Van Bemmelen. According to the latter, the West Progo Beds are for a part overlying the Old Andesites, for a part laterally merging with the higher strata of the latter. We may distinguish two facies;

The Jonggrangan marls and limestones: reef limestones with numerous bioherm and reef-formations, unstratified in themselves, intercalated in bedded limestones and lenses of marls. They contain numerous larger foraminifera, indicating a Lower Burdigalian age Te5-Tfl.

Partly overlying, partly laterally merging into this, we find a second facies:

The Sentolo Beds (Formation). These beds are overlying older volcanics with a basal horizon of volcanic agglomerates and marls, with few foraminifera. On some places corals are found in the Sentolo Beds, indicating, an age similar to the Jonggrangan Beds, but in some places they may be younger. The basal layers (125-250 m) pass upwards into well bedded limestones with a neritic facies. In the Gunung Sewu and near Wonosari (40 kms SE of Yogyakarta) these limestones pass into a series which is there called Wonosari Limestones (see Southern Mountains Miocene) containing a fauna of' foraminifera and corals [Osberger (1954) similar to the fauna of the Jonggrangan Beds.

The stratigraphical relationship between Sentolo and Jonggrangan Beds is therefore not yet clear.

After the deposition of the West Progo beds the area was uplifted to form the Southern Mountains (Gunung Kidul, Gunung Sewn) of South Central Java.

Type locality: West Progo Mountains, West of Progo River, W of Yogya, Central Java.

Geographical distribution: West Progo Mnts, Southern Mountains, Central Java.

Diagnostic fossils: Flosculinella globulosa, F. bontangensis (Rutten), Lepidocyclina marginata Michelotti, L. flexuosa Rutten, Miogypsina thecidaeformis Rutten, M. kotoi Hanzawa, Miogypsinoides (Miogypsinella?) Cycloclypeus annulatus Martin, Trillina howchini (Schlumberger).

References: Bemmelen (R.W. van) (1949), pp. 596-598 Osberger (1954).

Bemmelen (R.W. van) (1949. The Geology of Indonesia, vol. 1,,1, pp. 586-587.

"Sandy Globigerina Marls, with some glauconite sandstone Beds. Platy, sandy limestones and calcareous sandstones. Thickness about 700 in." Because of the lack of data, mostly unpublished and collected by oil companies (B.P.M.) no details can be told about this formation. It wits originally considered to be Upper Miocene, because of the occurrence of Lepidocyclina, but there exists a tendency to include at least part of' the Pliocene in formation. The Wonocolo Formation is developed in the Southern part of the Kendeng anticlinoriuin (Cepu oilfield) but seems to be represented by a stratigraphical gap in the N (Rembang). With the uplift and erosion of the Rembang Zone (now the zone of older Miocene outcrops) in latest Miocene times the Wonocolo was stripped from the area, as was most of the underlying Ngrayong formation and localy older formations.

The formation overlies the Rembang Formation, and is in turn overlain by the Ledok Formation, the former of late Miocene, the latter of Pliocene age. Possibly the formation may be in part correlated with the Lower Kalibeng Formation (Globigerina Marls).

Type locality: not mentioned.

The type locality where this formation originally has been described from, almost certainly must be somewhere in the neighbourhood of the tiny village of Wonocolo, on the western part of the Kawengan anticline.

It might be observed that the boundary Pliocene-Miocene still has to be established in East and Middle Java.

Geographical distribution: In cores of anticlines in the Cepu area between Blora and Cepu, N part of Central Java, an area of about 50 km in E-W direction and 40 km in N-S direction.

Diagnostic fossils: Lepidocyclina sp. ?

Reference: Bouwer 1957/66, Bemmelen (R.W. van) (1949b), pp. 33-34.

See: Southern Mountains Miocene.

See: Jiwo Layers.