Bemmelen (R.W. van) (1938). De Ringgit Beser. Nat. Tijdschrift Ned. Indie, t. XCVIII, pt..4, pp. 171-194.

Volcanic pumice layers, beginning with a basal conglomerate and ending with a pumiceous breccia of white pumice and black scoriaceous basalt.

The Bagor layers are overlying older layers of the Ringgit Beser complex.

Type locality: Bagor Mnts, between Bondowoso and Situbondo, N. Coast E. Java.

Geographic distribution: Ringgit-Beser volcanic complex and environments, idem.

Reference: Bemmelen (R.W. van) (1949a), p. 552.

See: Oostingh'S MOLLUSCAN STRATIGRAPHY OF NEOGENE.

Bemmelen (R.W. van) (1938). De Ringgit-Beser. Nat. Tijdschr. Ned. Indie, vol. XCVIII, pt. 4, pp. 171-194.

Erosion products of the leucite-bearing Ringgit Volcano, deposited during Lower Pleistocene times. The qualification "Horizon" (= zone) should not be applied in this connection.

Type locality: Batungampur, near G. Beser, SE of Besuki, N Coast of East Java.

Geographical distribution: a narrow strip, running about EW, N of the G. Djembur - G. Beser over a length of about 10 km.

Reference: Bemmelen (R.W. van) (1949), p. 552.

Brouwer, J. (1957, isued 1966). Stratigraphy of the younger Tertiary in North East Java and Madura. Bataafse Int. Petrol. Maat. n.v. The Hague. Report EP-37680.

Pleistocene terms used by the B.P.M. were as follows:

Lidah Formation

Malo Limestone Member (= upper part of Turi Fm of van Bemmelen)

Domas Tuffaceous Sandstone Member (= Lr. Turi Fm of van Bemmelen)

Lidah Clay Member

LIDAH FM. Author: Van Gogh, 1906, Blue grey clays in the vicinity of the Lidah Anticline. Volcaniclastics, sandstones and limestones elsewhere.

Malo Limestone Member. A minor limestone unit with patchy distiribution. It as been seen in outcrop in the Kawengan area (near Malo vilage, Makkinga 1934), and in shot-point samples to the east, where it is seen to be composed of molusc debris and some foraminifera.

Haar (C. ter) (1929). Excursion guide E4, 4th Pacific Science Congress, Java.

The beds consist of the following four units:

4. Vertebrate-zone. This higher unit consists of terrestrial sandstones and conglomerates with scattered vertebrate remains.

The lower part consists of volcanic tuffs, sands and conglomerates, at the base alternating with marine deposits.

(Globigerina-marls and pelecypod shells, very shallow water deposits). The combination indicates a beach deposit, where vertebrate remains from rivers or creeks were deposited in a neritic-littoral environment.

3. Turritella zone, clayish Globigerina-beds with marine pelecypods.

2. Breccia zone, andesitic pyroclastic sediments with marine intercalations.

1. Limestone-marl zone with small forms of Lepidocyclina (Trybliolepidina).

The superposition given above is according to that found in the field 1 = lowest, 4 = uppermost bed.

The age of the limestone-marl zone is Upper Miocene, zones 2 and 3 are considered to be of Pliocene age.

The vertebrate zone, containing the Kali Glagah fauna of von Koenigswald, is considered to be lowermost Pleistocene by Marks (1957).

Comments from Prof. G.H.R. von Koenigswald:

"The vertebrate zone of the Kaliglagah lies in Oostingh's Cheribonian. If Kaliglagah is made Pleistocene, the same must happen to the Cheribonian."

Type locality: Kali Glagah, near Bumiayu, S. of Tegal, Central Java.

Geographic distribution: Type locality only.

Diagnostic fossils: Mastodon (Trilophodon) bumiajuensis V.D. Maarel, Hippopotamus simpler, Colossochelys atlas. (Vertebrate Zone).

References: Zwierzicky (J.) (1926), pp. 229-234; Maarel (F.H. van der) (1932); Koenigswald (G.H.R. von) (1933), no. 23; Bemmelen (R.W. van) (1949), pp. 91-92.

Bemmelen (R.W. van) (1941). Toelichting bij Bladen 73 (Seinarang) en 74 (Oengaran), Geol. kaart van Java, 1/100.000, pp. 38-45.

The Damar Series consists of four parts, sometimes including intermediary layers, forming the upward passage from the marine neritic Kalibiuk Beds to the Damar Series proper, which has a terrestric facies. This passage is characterized by a zone of intertonguing, which zone may have a thickness varying between 0-600 m. The intermediary layers consist of grey and black clays, often with small marly concretions; intercalations of tuffaceous sandstones and pebble beds, and some lignitic beds. The tuff-sandstones are little hardened, and contain freshwater molluscs comparable with those of the Kali Glagah Beds in the W part of the N Serayu Range.

A section is described from the Kripik river, S of the village of Sukorejo:

Overlying the Kalibiuk marls and clays, with on top a bed of calcareous tuff marl, containing thick-shelled marine molluscs are

1. Intermediary layers (transition zone).

Black clay with calcareous concretion, and a tuff-sandstone with marine molluscs. Upwards the clay contains more and more intercalations of tuffaceous sandstones and conglomerates, with Melania (brackish water). On top lie basal conglomerates of the Lower Damar Beds.

2. Lower Damar Beds: At the base they consist of one or several layers of conglomerates of polymict composition with a calcareous cement. Then follow tuffaceous sandstones and conglomerates of andesites, partly cemented by calcareous material, partly uncemented. Together with the Intermediary Layers, the thickness may attain 800 m. They may be correlated with the Kali Glagah Beds from the Bumiayu region.

3. Middle Damar Beds. Augite-olivine basalt breccias of varying thickness. In the South the M. Damar Beds are represented by lahar deposits.

Towards the N, in the Candi hills of S Semarang, an intercalation of fluviatile, cross-bedded tuffaceous sandstones, conglomerates and lapilli-tuffs, divides the coarse breccias into a lower and an upper division. The thickness of the coarse breccias diminishes towards the N. while the thickness of the fluviatile deposits increases in the same direction. These M. Damar Beds may be correlated with the Mengger Horizon in the Bumiayu District. The thickness is about 150 m.

4. The Upper Damar Beds. Conformably on top of the Middle Damar Beds follow tuffaceous clays, sandstones and conglomerates, with local intercalations of lahar deposits. The conglomerates have a basaltic composition, while the tuffs are andesitic. These conglomerates are not cemented, or only locally so. The thickness is about 100 m or more.

A fragment of a molar of Elephas namadicus has been found, indicating a correlation with the Gintung Beds of Bumiaju, or middle-upper Pleistocene. (Kabuh Beds of the Kendeng Hills - Solo Plain to the west).

The Upper Damar Beds are unconformably overlain by the Notopuro Beds (Formation).

Type locality: Kali Damar, South of Weleri, Northeast of Central Java.

Geographical distribution: Along the entire N rim of the N Serayu Mnts; the Candi Hills, S of Semarang, in the areas of Bodri, Garang and Penkol, all in Central Java, Semarang area.

Diagnostic fossils: Elephas namadicus (see text).

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

Bemmelen (R.W. van) (1949). The Geology of Indonesia, vol 1A, p. 610.

Volcanic deposits consisting mainly of breccias of augite-hypersthene andesite, olivine basalt, and hornblende andesites, erupted by the volcanic G. Rogojembangan and overlying the upper Pliocene Ligung Series.

The beds were first distinguished as a separate unit by van Bemmelen in 1949, but they were already described as the "volcanics and volcanic ruins" of the "Jembangan Mnts". by the same author in 1937.

According to this author, the Jembangan Beds are to be correlated with the Linggopodo Beds (from Slamat and Cowet volcanoes) to the West, and with the Notopuro Beds (from Unggaran volcano) to the East.

Type locality: Gunung (= Mountain) Rogojembangan, 10 km E of Pananggaran, Karangkobar district, border of the residencies Pekalongan and Banyumas, Central Java.

Geographical distribution: Slopes of the G. Rogojembangan and adjacent volcanic mountains, Geological Map of Java, 1: 100,000 sheet no. 66.

Diagnostic fossils: None.

Reference: Bemmelen (R.W. van) (1937), p. 26.

Bemmelen (R.W. van) (1938). De Ringgit-Beser. Nat. Tijdschrift van Ned. Indie, vol. XCVIII, pt. 4, pp. 171-194.

Volcanic layers erupted by the Ijang volcano, of mainly basaltic composition.

The Jembur Layers are overlain by the Bagor Layers (Formation) and are overlying the Batungampur Horizon.

Type locality: Gunung Jembur, 15 km SE of Besuki, N. Coast of East Java.

Geographical distribution: Ringgit-Beser volcanic complex, between Bondowoso and Situbondo, East Java.

References: Bemmelen (R.W. van) (1949), p. 552.

Haar (C. ter) (1934). Toelichting bij Blad 58 (Boemiajoe). Geol. Kaart van Java, 1 / 100,000, pp. 33, 34, 40.

Coarse andesitic conglomerates, alternating with greenish grey sandstone, sandy claystone and clay, the latter characterized by the presence of concretionary layers of calcareous sandstone and numerous small white concretions of marly composition. The conglomerates are quite coarse and contain silicified or carbonized wood, as well as badly preserved vertebrate remains. In the upper part of the formation intercalations of white tuffs occur. Along the Kali Gintung the total thickness of the beds is about 800 m. As they are situated well above the Lower Pleistocene Upper Vertebrate Zone (see: Kali Glagah Beds) and overlie conformably the Mengger Horizon (Formation), a Middle to Upper Pleistocene age may be assumed for the Gintung Beds. The Gintung Beds contain pebbles of typical fibrous limestone, as well as sandstone and marl, probably from the underlying Pemali and Rambatan. Beds. These beds must therefore be disconformably overlain somewhere in the vicinity, although in the type region the Gintung Beds follow with apparent conformity on top of the preceding formations.

The Gintung Beds are correlated with the Upper Damar Beds of the Western Kendeng. by van Bemmelen. They may possibly be also correlated with the Kabuh Beds of the Central and Eastern Kendeng Mnts

Type locality: Kali Gintung (a small river), a tributary of the Kali Jurang (Cijurang), at long. 108° 58' 50" E, lat. 7° 11' S, W Java.

Geographical distribution: An area of 6 sq. km to the E and W of the type locality, and a second area of about 4 sq. kin in the centre of the syncline of Igir Cabe, 4 km to the SW of the type locality (W Java).

Diagnostic fossils: None mentioned.

Reference: Bemmelen (R.W. van) (1949a), p. 607.

Duyfjes (J.) (1936). Zur Geologic und Stratigraphie des Kendenggebiestes zwischen Trinil und Soerabaja (Java), De Ing. in Ned. Indie, vol VIII pt. IV, pp. 136, 137, 139, 143, 147.

Coarse grained, volcanic sandstones and conglomerates, containing fresh-water molluscs and vertebrate fossils of the Trinil fauna. (Middle Pleistocene). In the most Eastern part marine intercalations occur (near Surabaya).

The Kabuh formation conformably overlies the Pucangan formation, and is in turn disconformably overlain by the Notopuro formation, or by Holocene deposits. S of Sidoarjo (sheet 116) they are overlain by the volcanic Jombang formation.

Type locality: The formation is named after a village Kabuh (Kaboeh) 18 km N of the small town Jombang, on sheet 110, geol. map of Java 1/100,000. The type section is not expressly indicated, however, so that we propose a section described in some detail in Kali Sumberingin (Soemberingin), 3.5 km East of Kabuh, long 112° 14' 47" E (5° 26' 20" E of Jakarta meridian), lat. 7° 23 45" S. The section is a follows:

Holocene deposits.

Coarse and fine sandstones 90 m

Pebble beds with vertebrate fossils 10 m

Coarse and fine sandstones 140 m

Yellowish brown breceious tuffsandstone with Placuna and Ostrea (Marine) 5 m

Coarse sandstones and tuffaccous sandstones 50 m

Black clay with Melania 5 m

Total thickness 300 m.

Pucangan formation: Conglomerates with vertebrate fossils of Jetis fauna, etc.

Geographical distribution: In several small anticlines about 15 km N of Surakarta: Sangiran anticline, Gemolong anticline (von Koenigswald, 1940; van Bemmelen, 1949, p. 569). Further in a continuous strip along the Kendeng Hills (Anticlinorium) over 200 km in WE direction, between the towns of Semarang and Surabaya.

Diagnostic fossils: Trinil Fauna of von Koenigswald (1934). Cervus lydekkeri Martin: Duboisia kroesenii (Dubois); Mececyon trinilensis Stremme; Stegodon trigonocephalus Martin; Elephas cf. namadicus Falconer: Sus macrognathus Stremme; Sus brachygnathus DuBois; Hippopotamus namadicus Falconer; Bos bubalis paleokerabau DuBois; Pithecantropus erectus DuBois.

References: Duyfjes (J.) (1.938a), pp. 36-40; Duyfjes; (J.) (1938b), pp. 45-52; Duyfjes (J.) (1938c), pp. 50-54; Duyfjes (J.) (1938d), pp. 35-41; Koenigswald (G.H.R. von) (1934), pp. 181-201; Koenigswald (G.H.R. von) (1940); Bemmelen (R.W. van) (1949a), pp. 93, 96, 566, 575,576,577,581.

Martin (K.) (1900b). Eintheilung der Tertiarschichten auf Java. Zeitschr. dtsch. geol. Ges., t. Lll, Verh., p. 8.

Originally this name was given by Martin to all vertebrate-bearing layers occurring in the Kendeng Mountains (East and Central Java). These beds were correlated with the Trinil-beds of DuBois (T.K.N.A.G., serie 2, XXV, 1908, p. 1235), an ossiferous bed of volcanic origin, occurring near Trinil, East Java.

The term given by DuBois to this complex of layers is Javanese Siwaliks (Versl. v.h. Mijnw., 3e kwart., 1890), as he believed them to correspond to the Siwalik series of India.

Originally Martin considered the age of the Kendeng beds as being Pliocene, while DuBois believed them to be Pleistocene.

Later research has proved that not all bone-bearing formations belong to the same age. Especially Duyfjes and von Koenigswald have done much to establish a stratigraphy of the bone-bearing formations. It is desirable, however, to keep the name "Kendeng Beds" (group) as a collective name for those layers of Pleistocene age, which may locally contain a fossil vertebrate fauna, and which are mainly restricted to the Kendeng Hills and the adjacent areas of East and Central Java.

As such, the Kendeng Beds are a series of mixed volcanic, fluviatile, limnic and rarely marine layers, with relatively rapid lateral facies changes, while the thicknesses are rarely constant over some distance. They represent the sedimentation in a rather well-defined area with strong volcanic activity in and slow uplift of the surrounding regions, the area itself remaining a sedimentary basin with in some parts (Kendeng Hills) geosynclinal tendencies.

One may distinguish four separate formations:

4. The Solo terraces (Ngandong layers). Sands and gravels covering the slopes of the hills, especially along the Solo-river between Ngawi and Cepu, on levels varying between 38-71 m over sea-level (The river bed is at about 38 m) representing deposition during a progressive rise of the Kendeng-Hills while the river was cutting in antecedently. On many places the gravels contain vertebrate remains including Solo-Man (Homo neanderthalensis soloensis (Oppenoorth), e.g. in Ngandong and Watualang. (Ngandong fauna, v. Koenigswald). Age: Uppermost Pleistocene.

The underlying deposits show distinct West-East facies changes:

3. The Notopuro - Jombang layers (formation). Along the entire length of the Kendeng Hills these consist of andesitic breccias and agglomerates, locally in the form of lahar-deposits. In the Western Kendeng Hills (between Ungaran and Ngawi) as well as in the central part (between Ngawi and Jombang) they contain a vertebrate fauna, mainly consisting of rolled and ? unrolled specimens of the Trinil Fauna.

In the eastern part sediments in the same position are called the Jombang layers, the basal strata of which are marine, passing upward into volcanic andesitic breccias derived from the ancient Willis volcano. In the western part of the eastern section the marine layers are thin, growing thicker towards the east. This is interpreted as a seaward growing of the foot of the volcano, crowding out progressively the marine sedimentation. No vertebrate remains have as yet been encountered in this part. Max. thickn. of both form. 300 m.

Age: Upper Pleistocene (q. v. separate description).

2. The Kabuh beds (Formation). Cross-bedded andesitic sandstone and gravel with intercalations of andesitic tuff, sometimes with a basal conglomerate. The layers are the result of erosion in neighbouring areas, especially towards the west and south. The thickness varies from about 50 m in the west (Sangiran) to several hundreds of meters in the eastern part.

In the central part of the Kendeng Hills intercalations of Globigerina marl occur, which are, however, the product of sedimentation in limnic surroundings, as is proved by the inclusion of fresh-water deposits. In the east the beds gradually pass into marine clays and marls (Sidoarjo). The strata contain a vertebrate fossil fauna (Trinil-fauna v. Koenigswald).

Age: M. Pleistocene

1. The Pucangan layers (Formation). Between Trinil and Ngawi they consist of volcanic breccias and lahar deposits, derived from the ancient Willis volcano. These volcanics dammed up the area to the West, which, originally a shallow marine basin, now resulted in a shallow lake. In this lake, extending southward towards Surakarta, black clays were deposited, especially well-exposed in the Sangiran anticline, 10 km N of Surakarta.

In these black clays an intercalation is found of a few meters thickness consisting of marine shallow water deposits, corresponding with an ingression of the sea. Another characteristic of the black clays is the presence of intercalations of nearly pure diatomaceous earth, indicating temporary brackish water conditions. -

The Pucangan beds contain a vertebrate fossil fauna (Jetis fauna von Koenigswald) .

Kendeng Beds. Remarks from prof. R. von Koenigswald. In the sense as used by DuBois and Martin this term comprises only the Trinil and Jetis layers. It is certainly not right to extend this antiquated term (now and suddenly) to include the Ngandong and Jombang beds. The Ngandong Beds are Upper Pleistocene, but certainly not uppermost Pleistocene. In general publications the author (v. K.) has identified them with the climax of Wurm 1.

Towards the east, the volcanic facies gradually changes into a marine series, with the volcanic part at the top thinning gradually to the east. This is explained by assuming that the Willis volcano gradually built its foot towards the east, crowding out the marine sediments (cf. Jombang layers).

The thickness varies between about 200 m in the west to about 1,000 m in the central section and the east.

The Pucangan beds conformably overlie the Kalibeng beds of Pliocene age.

Type locality: Kendeng Hills, between Surabaya in the East and Ungaran volcano in the West. The subdivisions have been called after small localities mainly in the Eastern part of the Hills; for which is referred to the separate treatment of each of the formations.

Geographical distribution: Kendeng Hills, Solo plain N of Surakarta (Sangiran-, Gemolong-, Onto anticlines).

See also separate formations.

Diagnostic fossils: See separate articles.

Bemmelen (R.W. van) (1938). De Ringgit-Beser. Nat. Tijdschr. van Ned. Indie, vol. XCVIII, pp. 171-194.

Marly tuff-sandstones and conglomerates, deposited in a marine environment. They are overlain by the Ringgit Series (Formation) and conformably overlie the marine sedimentary Menuran Layers.

Type locality: Leprak, 5 km East of G. Beser, 1 0 km N of Bondowoso, N part of East Java.

Geographical divtribution: a small area around type locality only.

Reference: Bemmelen (R.W. van) (1949), pp. 552-553.

Haar (C. ter) (1934), Toelichting bij Blad 58 (Boemiajoe). Geol. kaart van Java, 1 / 100,000, pp. 40-4 1.

Andesitic volcanic products from the old Slamat or Copet volcano (van Bemmelen, 1949a, p. 610) consisting of breccias, tuffs and lahar-deposits, disconformably overlying the folded Tapak, Kalibiuk and Glagah Beds (Formation) in the Bentarsari Basin and in the Bumiaju Basin. In the latter they are overlain by even more recent volcanics from the Slamat volcano. The composition of the formation resembles very much that of the Kumbang Beds (Formation), and it is probable, that they are the product of the same volcanism in a younger stage. The Linggopodo Beds may, according to van Bemmelen, be correlated to the Jembangan Beds of the central North Serayu Mnts., and the Notopuro Beds of the Western ditto, and the Kendeng Hills.

Type locality: Gunung Linggopodo, long, 108° 59' 27" E, lat. 7° 8' 30" S. 13 km N of Bumiaju.

Geographical distribution: An area E of the type locality, consisting mainly of the mountain G. Ujung timur, and with an EW length of 6, a NS length of 4 km further along the E rim of the Bentarsari basin and in a strip of several km length E of Majenang. As they can only be distinguished from the Kumbang Beds by their tectonic and stratigraphic position, shed from the Kumbang Beds by their tectonic and stratigraphic position, part of the outcrops of the latter may belong to the Linggopodo Beds.

Diagnostic fossils: none.

References: Hetzel (W.H.) (1935?, p. 39; Bemmelen (R.W. van) (1949a), p. 610.

Haar (C. ter) (1934). Toelichting bij Blad 58 (Boemiajoe) Geol. kaart van Java, 1 / 100,000, pp. 3 2-40.

Light gray tuffs and tuff-sandstones, with intercalations of conglomerates and thin stringers of magnetite-sand. The Formation is 150 m thick, and forms a distinct topographical ridge. It overlies the Kaliglagah Beds conformably, and is in turn conformably overlain by the Gintung Beds. The Mengger Horizon (Formation) forms the lower limit of the Pleistocene deposits in the sheet Bumiaju of the Geol. Survey. It possibly contains the Upper Vertebrate Zone (Obere Wirbeitierhorizont) of von Koenigswald, the fauna of which was only found in the shape of rolled fragments in some small rivers that cut in their upper reaches through the Mengger Formation.

Van Bemmelen, 1949, correlates the Mengger Horizont with the Middle Damar Beds of the Western Kendeng Mnts, which also mainly consist of volcanic deposits.

Type locality: Gunung Mengger, near the village Cisaat, 10 km NNW of Bumiayu, long. 108° 58' 27" E. lat. 7° 10' 30" S. Good outcrops are found in the river Cisaat, border between W and C. Java.

Geographical distribution: Area of about 6 sq. km around G. Mengger forming a more or less continuous ridge around the synclines of Cisaat, and between Cicacaban and Kali Pemali, sheet 58, 1 / 100,000, Java geol. Surv.

Diagnostic fossils: For fauna of Upper Vertebrate Horizon see Kaliglagah Beds (Formation).

Reference: Bemmelen (R.W. van) (1949), p. 607.

Terrace-deposits of Solo-River (C. Java) near Ngandon., N of Ngawi.

Duyfjes (J.) (1936). Zur Geologie und Stratigraphie des Kendenggebietes zwischen Trinil und Soerabaja (Java). De Ing. in Ned. Indie, sect. IV De Mijning., vol. VIII, pp. 137, 143, 147, 148.

Tuffs, tuff-sandstones, conglomerates and agglomerates from volcanic or derived volcanic origin, overlying conformably or with a slight erosional hiatus the Kabuh Formation. Towards the East, in the sheets 109, 110, 115 and 116 of the Geological Map of Java 1 / 100,000, a formation in a similar position has been called Jombang Formation, which has similar composition, and is probably essentially equivalent. Fossils are rare in an occurrence at Sangiran (Kalioso) N of Surakarta, some fragmentary remains of vertebrates have been found, which may have been derived from the underlying Kabuh Formation, which is in this locality disconformbly overlain by the Notopuro Formation.

In terraces along the Solo River, North of Ngawi, a rich vertebrate fauna of Upper Pleistocene age has been described by von Koenigswald. These terrace-deposits overlie the folded Pliocene disconformably. As the Notopuro and Jombang Formations have also been folded in Middle Pleistocene orogeny, the Notopuro formation may be slightly older than the terraces, while being younger than the Middle Pleistocene Kabuh Formation. On the other hand, the coarse, river deposit conglomerates and sandstones of the Notopuro, may indicate an essentially synorogenic facies, and the age more or less equivalent to the higher terraces of the Solo River. The Notopuro Formation is overlain by holocene volcanic or alluvial deposits.

Type locality: Village of Notopuro, 35 km ENE of Madiun, Central Java, just W of the Gunung Pandan.

Geographical distribution: Western part of the Kendeng Anticlinorium, mainly along its N slope, between the Gunung (Mntn) Pandan in the E to Semarang in the W, further in a number of small anticlines 15-20 km. North of Surakarta (Sangiran Anticline, Gemolong anticline).

Diagnostic fossils: none.

Reference: Bemmelen (R.W. van) (1949a), pp. 93, 566, 576, 610.

See: KALIGLAGAH BEDS (Formation), UPPER VERTEBRATE ZONE.

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.

Duyfjes (J.) (1936). Zur Geologie und Stratigraphie des Kendenggebietes zwischen Trinil und Soerabaya (Java). De Ing. in Ned. Indie, vol. VIII, pt. IV, pp. 136, 137, 138, 142, 146.

In this formation two facies may be distinguished: a marine clayey facies, and a volcanic tuffaceous to sandy facies. The latter is rich in vertebrate fossils.

The volcanic facies is developed in the Western part of the Kendeng Hills, while to the East more and more marine intercalations occur, so that near Surabaya the formation consists entirely of clays and volcanic tuffs with marine molluscs.

Three sections were described by Duyfjes in the original paper: The most eastern one is at Perning, N of Mojokerto, near the locality where Homo modjokertensis was found:

g. Tuff-sandstones 35 m

f. Marly-clayey tuff-sandstones with marine molluscs and echinoids (III molluscan zone) 10 m

e. Green Clay (locally developed) 5 m

d. Thick bedded coarse sandstoines with irregular lenses of conglomerates with boulders of andesite;

fine clay tuff is locally intercalated. The lower part contains thin bedded fine tuff-sandstone,

forming a passage to c. Fragments of vertebrate remains.

This part contained the skull of Homo modjokertensis.

Thickness: 100 m

c. Thinbedded, finegrained tuffsandstone with a varying content of clay 10 m

b. Marls and clayey, sometimes conglomeratic tuff-sandstones with marine molluscs and locally developed

coral-bioherms. Big andesite boulders occur (Molluscan zone II)

a. Thin tuff-sandstone bed and clayey tuff-sandstone, sometimes with marine molluscs and difficult to separate

from b. (Molluscan zone I ?) 25 m

Total thickness 200 m

At the Gunung Butak, 90 km W of the preceding locality,the following section was described:

d. Bedded tuffs and tuff sandstones 125 m

c. Tuff-breccia 75 m

b. Bedded tuffs and tuff-sandstones 40 m

a. Tuff-breccia 200 m

This upper part has been called Butak Beds by van Es, 1931, p. 99.

The volcanic upper member lies here on top of a marine lower member, called Ngronan Member (Ngronan Horizont): marly and calcareous volcanic tuff-sandstones, containing marine molluscs, thickness 100 m. The total thickness of the Pucangan formation is therefore 540 m. Even more to the West, at Trinil, the Pucangan Formation is represented by 100 m volcanic breccias, with local intercalations of sandstones, tuffs and tuffaceous black clays, with freshwater molluscs. The entire section at Trinil is therefore with freshwater molluscs. The entire section at Trinil is therefore non-marine.

In general the facies of the Pucangan formation is strongly variable. This is due to its genesis: the volcanic beds have been deposited by the Willis volcano, which in this time (Lower Pleistocene) was very active. The lower part of the volcano reached into the marine Kendeng Basin, where at the same time limestones and marine clays were deposited. The volcanic activity and the radius of the volcano increased during the time of deposition, so that the lower parts of the formation are marine over a larger distance than the upper parts.

In the transition area three marine molluscan zones have been distinguished, one at the base, one in the middle and one at the top of the formation. Not all three zones are represented everywhere, however.

The volcanic facies contains locally vertebrate fossils, which have been placed at the Lower Pleistocene by von Koenigswald (Jetis Fauna) (1934, pp. 190 ff).

In the Sangiran Dome the Pucangan Beds are developed as black clay with a rich vertebrate fauna, as well as numerous fresh water molluscs. Somewhat above the base (about 25 m) there occurs a thin marine intercalation in the black clays, formed by sands with marine molluscs, followed by beds of nearly pure diatomaceous earth.

The thickness of the black clays is about 300 m.

The Pucangan Formation overlies the Kalibeng Formation, and is in turn overlain by the Kabuh Formation.

Type locality: Gunung (Mnts) Pucangan, 20 km N of Jombang, E Java, 112° 17' 7" E, 7° 23' 10" S.

Geographical distribution: Along the entire length of the Kendeng Range, over an E-W distance of 200 km, in a strip along the S slope of a breadth varying between 0.5 - 5 km; further in the centre of the Sangiran dome, 15 km N of Surakarta, near the railway station Kalioso.

Diagnostic fossils: Manis palaeojavanicus DuBois; Epimachairodus zwierzyckii von Koenigswald; Stegodon trigonocephalus cf. praecursor V. K.; Hippopotamus (Hexaprotodon) antivirus von Koenigswald; Cervus zwaani von Koenigswald; Antilope modjokertensis von Koenigswald; A. cf. saatensis von Koenigswald; Leptobos cosijni von Koenigswald; Tapirus pandanicus DuBois.

References: Es (L.J.C. van) (1931); Koenigswald (G.H.R. von) (1934), pp. 185-200;.Koenigswald (G.H.R. von) (1935), pp. 67-70; Duyfjes (J.) (1938), p. 18-36; Duyfjes (J.) (1938a), pp. 16-45; Duyfjes (J.) (1938b), pp. 30-50; Duyfjes (J). (1938), pp. 15-35; Bemmelen (R.W. van) (1949a), pp. 93, 96, 98, 570, 574,579.

Bemmelen (R.W. van) (1938). De Ringgit Beser. Nat. Tijdsclirijft van Ned. Indie, vol. XCVIII, pt. 4, pp. 171-194.

Leucite-bearing volcanic beds erupted by the Pleistocene Ringgit volcono.

The series is overlying the Leprak Layers and is in turn overlaid by the Batungampur Horizon, erosion products of the Ringgit volcanics.

Type locality: Gunung Ringgit, halfway between Besuki and Situbondo, N. Coast of East Java.

Geographical distribution: Ringgit Beser volcanic complex between Bondowoso and Situbondo, N. part of East Java.

Reference: Bemmelen (R.W. van) (1949a), pp. 552.

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

An upper member consisting of blue clays with marls and shell-limestones (Malo member.), and a lower member consisting, of blue clays. Total thickness 300-400 m.

The stage overlies the Mundu Formation, and is in turn overlain by high terrace deposits. Possibly it may be correlated with the upper part of the Damar Formation, or upper part of the upper Kalibeng Formation including the Pucangan Formation, and the Kabuh Formation.

According to B.P.M. the stratigraphy the Turi Formation is equivalent to the Domas Formation of the Surabaya area and the volcanic facies of the Pucangan Beds, containing more sand and sandstones and also fossil vertebrate of Lower Pleistocene age (Jetis fauna of von Koenigswald).

Type locality: Not mentioned. Probably near Cepu, 50 km S of Rembang,in N Java.

Geographical distribution: Rembang - Cepu Anticlinorium between Demak, E of Semarang, in the West and Madura in the East, in several anticlines. The anticlinorial area is about 200 km long in E-W direction, and 60 km broad in a N-S direction between Rembang and Cepu; N Java.

Diagnostic fossils: Not mentioned.

Remark from B.P.M.:

Reference: Bemmelen (R.W. van) (1 949b), pp. 33-34.