Oligocene palynological succession from the East Java Sea

EKO BUDI LELONO1 & ROBERT J. MORLEY2,3*1LEMIGAS, Jl. Ciledug Raya, Cipulir Kav.109, Kebayoran Lama, Jakarta Selatan 12230,

Indonesia2Palynova Limited, 1 Mow Fen Road, Littleport, Cambs, CB6 1PY, UK

3Department of Earth Sciences, Royal Holloway University, Egham, Surrey, UK

*Corresponding author (e-mail: palynova@btinternet.com)

Abstract: Rich palynomorph assemblages have been obtained through a marine Oligocenesuccession from the East Java Sea (Indonesia) and provide the first instance of an independentlydated Oligocene succession from SE Asia that has yielded a good quality palynological record.The succession has been independently dated by nannofossils and foraminifera.

The palynomorph succession suggests climatic control on Oligocene vegetation, on which basisa regionally applicable zonation is proposed. The Early Oligocene is characterized by common rainforest elements, suggesting an everwet, rain forest climate. The early part of the Late Oligocenecontains much reduced rain forest elements with grass pollen, indicating a more seasonalclimate, whereas for the latest Late Oligocene, rain forest elements return in abundance, suggestinga superwet rain forest climate. This palynological succession is similar to that from the SundaBasin in the West Java Sea, allowing the Sunda Basin succession to be dated by correlation.

The study also extends the stratigraphic range of Dacrydium and Casuarina, two plant taxapreviously thought to have dispersed from the Australian Plate into SE Asia at the time of thecollision with Sunda, to well before the time of collision. A different means of dispersal forthese taxa is proposed.

The area of study is located on the off-shore of NorthMadura which is a part of the East Java basin(Fig. 1). This is a back-arc basin situated on thesouthern margin of the Sundaland. This basincovers an area over 54 000 km2 with an east–westalignment and accommodates sediment with athickness of more than 2000 m (Pusoko et al. 2005).It is well known as an important hydrocarbon pro-vince in Indonesia. East Java has been an attractivearea for oil exploration and new discovery continuesto occur within this basin.

A regional stratigraphy of the East Java basinis shown in Figure 1. The stratigraphic successionfollows an internal Lemigas report and alsoYulianto et al. (2000). Sedimentation commencedduring the Middle Eocene, unconformably overCretaceous metasedimentary and igneous base-ment rocks and Paleocene/Late Cretaceous ‘Pre-Ngimbang’ sediments, with deposition of theNgimbang Formation. The Ngimbang Formationconsists of sands, coals and lacustrine shales in thelower part, and subsequently marine shales andlimestones deposited during the Late Eocene andEarly Oligocene, and forming the synrift phase ofdeposition within the basin.

Subsequently, following a period of non-deposition/erosion during the mid Oligocene, dur-ing a period of post-rift tectonic quiescence, thick

and extensive carbonates of the Kujung Formationformed over the major part of the area during LateOligocene–Early Miocene (Johansen 2003). Thiswas followed by clastics of the Tuban Formationduring the latest Early Miocene.

The Kujung Formation is divided into threeunits, generally termed Kujung Units III, II and I.Kujung unit III is the oldest (Late Oligocene) andconsists of alternations of shale, sand and limestone.Kujung unit II is characterized by clastics and car-bonates with a basal sandstone and formed duringLate Oligocene–Early Miocene, whilst Kujungunit I is represented by widespread Early Miocenecarbonate build-ups.

The Kujung Formation is conformably overlainby the Tuban Formation which is dominated byclaystones with the intercalation of foraminiferal-rich marls forming during the Early Miocene in adeep shelf setting (Firdaus 2004), and includesthe widespread Rancak reef limestone member.The younger Neogene succession consists of theNgrayong, Wonocolo, Ledok and Mundu For-mations.

The Oligocene of the East Java Sea area isusually subdivided biostratigraphically using acombination of nannofossils and foraminifera. It isindeed one of the mainstay areas for larger forami-nifera, with many classic papers from the onshore

From: Hall, R., Cottam, M. A. & Wilson, M. E. J. (eds) The SE Asian Gateway: History and Tectonicsof the Australia–Asia Collision. Geological Society, London, Special Publications, 355, 333–345.DOI: 10.1144/SP355.17 0305-8719/11/$15.00 # The Geological Society of London 2011.

region (Van der Vlerk & Umgrove 1927; Leupold &Van der Vlerk 1931), and also for planktonic fora-minifera (Bolli 1966). In the area NW of Madura,however, the Kujung Formation often containsinterbedded clastics which introduce additional cor-relation problems, and to try to clarify correlationsin this area well sections have been studied for pal-ynology as well as the usual microfossil groups.Samples from two wells, termed Well X and WellY, have been studied at 600 intervals for each dis-cipline, with some analyses of sidewall cores.

The traditional palynological zonation for SEAsia (Morley 1978, 1991) does not work well inthis area, and so the succession has been dividedinto broad palynological assemblage zones, whichappear to be controlled mainly by climate. Somepollen types previously found to be stratigraphicallyuseful in the Sunda Basin have also been recorded,and can be used in this area to help define thezones. The palynological zones appear to providethe best criteria for correlation of the observedstratigraphic succession between the two wells.

The age of the assemblage zones, however, isbest determined on nannofossils, with support fromlarger foraminifera. This provides one of the firstinstances where an Oligocene palynological succes-sion from the SE Asian region can be independentlydated using marine fossils. For nannofossils, refer-ence is made to the scheme of Martini (1971) aspresented by Perch-Nielsen (1985). For planktonic

foraminifera, the scheme of Blow (1969, 1979) isfollowed using taxon ranges as presented by Bolli& Saunders (1985), whereas the larger foraminiferalzonation follows Adams (1970). The timescale usedis that of Gradstein et al. (2004).

Based on the close similarities of the palyno-logical succession with that from the Sunda Basin,it is possible to apply at least part of the zonationscheme in the non-marine Sunda Basin Talang Akarand Cibulakan Formations, thus providing the firstdirect indication of the age of these formations.

Apart form providing a new, independentlydated, palynological zonation this paper will alsodiscuss the regional implications of the climaticsuccession The sequence is also characterized bythe common occurrence of palynomorph taxa ofAustralasian origin, and the biogeographical impli-cations of these records are considered.

Overview of datasets

The datasets are reviewed by discipline, in relationto the lithostratigraphic succession.

Foraminifera

The succession yields variable recovery of fora-minifera, consisting mainly of calcareous bentho-nics (Fig. 2), with larger foraminifera featuring

Fig. 1. Location and lithostratigraphic succession. Arrow indicates interval studied. Stratigraphy from internalLEMIGAS report, Onlap curve from Vail et al. (1977) and Haq et al. (1988).

E. B. LELONO & R. J. MORLEY334

prominently. Planktonics, however, are poorlyrepresented.

With respect to planktonics, the presence ofGlobigerina tripartita and Globorotalia opimanana in Well X indicates reference to the LateOligocene Planktonic zone P22, but correlation toWell Y cannot be achieved as planktonics in thatwell are very rare indeed.

Larger foraminifera provide a better basis forcorrelation (Fig. 2), since Lower Te foraminifera(Spiroclypeus spp without Miogypsina spp) are wellrepresented in both wells. The Early Oligocene TcLetter stage is represented in Well Y from theregular presence of Nummulites fitchelii, but not inWell X. However, the occurrence of Tb markerNummulites variolensis near the base of the well,although present in both sections, may be due toreworking (see below).

Nannofossils

Nannofossil recovery from both sections was goodin the upper part, and zone NP25 can be interpretedfrom the interval between the highest occurrenceof Sphenolithus ciperoensis and the highestS. distentus (Fig. 3). The base of NP24 ismarked by the deepest occurrence of Sphenolithusciperoensis, but this species appears much lower

stratigraphically in Well Y, where it is likely to bepresent closer to its true base. Its base in Well X islikely to be controlled by environmental constraints.

There are no nannofossils to date the Early Oli-gocene, although the topmost Eocene nannofossilDiscoaster saipanensis (top in NP20) occurs at thebase of both wells, for which reworking is sus-pected. Eocene foraminifera and nannofossils areassociated with a basal lag over basement in bothWell X and Well Y. Foraminifera include Globora-taloides carsoseleensis (tops in P16) and Morozo-vella lehneri (tops in P14) and Cribrohantkeninainflata (range P16/17) together with the Tb largerforam Nummulites variolensis. The Eocene assem-blage is thus from a variety of different stratigraphicintervals, with taxa with ranges that do not overlap.The likelihood is that the basal lag contains amixture of reworked Eocene fossils and may be ofEarly Oligocene age. The rarity of palynomorphmarkers for top Eocene would also support theidea that Eocene sediments are missing from thesesections.

Palynology

Rich pollen and spore assemblages were found moreor less throughout the succession, and dinoflagellatecysts and other marine palynomorphs were also

Fig. 2. Foraminifera from Well X and Well Y, identifications by LEMIGAS.

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well represented. Pollen/spore assemblages can bedivided into three groups, mangroves, hinterlandpollen and spores. The hinterland pollen groupshows the most interesting succession, with ele-ments on the one hand suggesting everwet climates(Table 1), and seasonal elements on the other(Fig. 4). Mangrove pollen however suggests strongenvironmental control since mangrove pollenshows different abundance variations in the twowells. Pollen is compared to that of modern taxawhere appropriate, with the suffix ‘type’ beingadded in instances when a pollen type compares tothat of more than one extant taxon. A list of the paly-nomorph taxa mentioned in the text and theirrespective morphotaxon names is given in Table 2.The palynological slides from which assemblageswere recorded are stored at LEMIGAS StratigraphyUnit, Jakarta.

Dacrydium and Casuarina:superwet elements. Thehinterland pollen group shows pollen of Dacrydiumand Casuarina type (Fig. 5) to be particularlywell represented in the upper part of the succes-sion. These taxa are of Gondwanan origin, and fol-lowing dispersal into the SE Asian region foundniches in peat swamps and Kerangas vegetationor ‘heath’ forests (Gymnostoma spp), montaneforests (Dacrydium spp and Casuarina junghuhni-ana) and also along beaches (Casuarina equisi-tifolia). The occurrence of abundant Casuarinatype and Dacrydium pollen in the Well X andWell Y wells suggests a peat swamp derivation

(e.g. these pollen types are common in coals fromthe laterally equivalent ‘Coaly’ Talang Akar For-mation in the Sunda Basin, Morley 2000). Casuar-ina/Gymnostoma and Dacrydium do not occur in

Fig. 3. Nannofossils from Well X and Well Y, identifications by LEMIGAS.

Table 1. Tropical moist climates

Constant high temperature is characteristic of tropicalclimates, and climates in which the mean temperatureof the coldest month is 188 or over is often used as adefinition (Whitmore 1998), but the absence of frostswas shown to be a critical factor by Morley (2000).Also, the mean diurnal temperature range exceeds theannual range. Everwet, or perhumid tropical climatesoccur in those areas with typically more than2000 mm of rain per year and where every month iswet (with 100 mm of rain or more) but there may befrequent short dry periods or a very short dry season(Richards 1996) and such climates permit thedevelopment of true evergreen rain forests. The term‘superwet’, for climates in which dry periods are rareor absent and in which annual rainfall exceeds3000 mm was proposed by Richards (1996) and froma geological standpoint is useful since such climatesmay permit growth of true ombrotrophic peats.Tropical wet seasonal climates may have a significantdry season of up to 4 months with less that 100 mmof rain per month (Richards 1996). Areascharacterized by soils exhibiting a slight moisturedeficit during the dry season may supportsemi-evergreen rain forests, whereas areas with astrong soil water deficit would support monsoonforest (Whitmore 1998).

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Fig. 4. Mangrove, hinterland pollen and Dacrydium/Casuarina from Well X and Well Y. Main components of palynomorph assemblage groupings as follows: ‘Backmangrove’,Sonneratioid and Brownlowia pollen; Nypa (in blue) ‘Coastal’, Terminalia, Thespesia, Barringtonia pollen; ‘Rain forest’ pollen of Dipterocarpaceae, Burseraceae, Leguminosae andmany others; ‘Kerapah’, Casuarina and Dacrydium pollen; ‘Peat swamp’, Blumeodendron, Cephalomappa, Calophyllum, Durio and Sapotaceae pollen; ‘Seasonal’, Poaceae pollen;‘Montane’, mainly Podocarpus pollen. The groups reflect the main vegetation types from which the fossil pollen is thought to be derived – the taxa are not wholly restricted to thevegetation types indicated.

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the communities of the domed topotrophic/ombrotrophic peat swamps which are widespreadalong the coasts of Kalimantan and Sumatra (e.g.Anderson 1963), but characterize the less wellknown ombrotrophic (blanket bog type) ‘Kerapah’or watershed peats which occur locally in Borneoon poorly drained podsolic soils (Brunig 1990;Morley 2000) in areas of ‘superwet’ climate(Richards 1996). The occurrence of ‘Kerapah’swamps is thus convincing evidence for aneverwet climate (Fig. 4).

Riparian elements. Pollen of riversides and alluvialswamps, especially of Pandanus and Ilex (Figs 5 &6), show distinct trends, being common in thetopmost part, above the interval with commonDacrydium pollen, and also common in the intervalwith regular seasonal climate elements (see below).

Seasonal climate elements. The regular occurrenceof Poaceae (Fig. 5) and Schoutenia pollen (Schoute-nia is an element of seasonal evergreen forest) in themid part of the succession suggest a more seasonalclimate aspect to the mid part of the succession.This interval is also characterized by the regularoccurrence of Malvacipollis diversus, which com-pares closely with modern pollen of AustralianAustrobuxus swainii and Dissiliaria baloghioides(Martin 1974), and differs from SE AsianAustrobuxus spp in its shorter spines and smallersize. These are both trees of modern drier rainforests/warm temperate sclerophyll communities

in SE Queensland/NW New South Wales (Pickettet al. 2004).

Algal and other marine palynomorphs. Dinoflagel-lates are common through both wells and consistmainly of Operculodinium spp, Spiniferites sppand Homotryblium spp, but without useful age-indicative taxa. However, the dinoflagellate cystsdo show two distinct acmes in the mid part of thesuccession (Fig. 7). There is one very strong acmewithin both wells, with abundant Operculodiniumspp and Spiniferites spp, and below this a secondless pronounced acme of the same taxa, but alsowith common Homotryblium spp. These acmes arecoincident with the events based on hinterlandpollen discussed above.

Palynological zonation scheme

The main palynological events are brought togetherin Figure 7, and five zones are proposed in the basisof assemblage changes as follows:

Zone OL-1. This zone is difficult to define, and isbased essentially on the rarity of seasonal climateand riparian elements.

Zone OL-2. This zone is characterized by the regularoccurrence of seasonal climate elements, especiallyof Malvacipollis diversus (Fig. 5), with the top con-tinuous occurrence of this species marking the topof the zone. Other seasonal climate elements are

Table 2. Pollen types and pollen morphotaxa from Java Sea wells

Pollen type Morphotaxon Family

Arenga type Arengapollenites sp ArecaceaeAustrobuxus swainii/Dissiliaria

baloghioidesMalvacipollis diversus Harris

(1965)Euphorbiaceae

Canthium type Canthiumidites sp RubiaceaeCasuarina type (Casuarina/

Gymnostoma)Casuariniidites cainozoicus

Cookson & Pike (1954)Casuarinaceae

Crudia Striatricolpites catatumbusGonzalez Guzman (1967)

Leguminoseae

Dacrydium Lygistepollenites florinii Stover &Evans (1973)

Podocarpaceae

Eugeissona insignis type Quilonipollenites sp ArecaceaeEugeissona minor Quilonipollenites sp ArecaceaeIlex Ilexpollenites spp AquifoliaceaeMyrtaceae Myrtaceidites spp MyrtaceaePandanus Pandaniidites spp PandanaceaePinus Pinuspollenites spp PinaceaePoaceae Monoporites annulatus van der

Hammen (1954)Poaceae

Pometia SapindaceaeSchoutenia Echitriporites schoutenioides Tiliaceae

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Fig. 5. Pollen from Wells X, and Y, and from Talang Akar Formation. (1) Pometia pollen; (2, 3) Ilex pollen; (4)Casuarina type pollen; (5) Dacrydium pollen; (6) Pandanus pollen; (7) Myrtaceae pollen; (8) Poaceae pollen; (9)Schoutenia pollen; (10, 11) Malvacipollis diversus. Black line ¼ 10 microns.

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Fig. 6. Riparian and seasonal climate pollen from Well X and Well Y. See caption to Figure 4 for explanation of pollen groupings.

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Fig. 7. Palynomorph taxa used to zone the succession in Well X and Well Y, including total marine dinocysts.

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Gramineae pollen and Schoutenia pollen. Riparianelements are also well represented in this interval.

Zone OL-3. Zone OL-3 is characterized by commonto abundant Dacrydium and Casuarina type pollen,with a strong acme of dinoflagellate cysts dominatedby Operculodinium spp and Spiniferites sppmarking the top of the zone but the low represen-tation of Pandanus, Ilex and other riparian elements.

Zone OL-4. Zone OL-4 is characterized by abundantDacrydium and regular Casuarina type pollen, butthe low representation of Pandanus, Ilex and otherriparian elements and dinoflagellate cysts.

Zone OL-5. Zone OL-5 is characterized by reducedDacrydium and Casuarina type pollen, and in-creased riparian elements such as Ilex and Pandanus.

Climate history

Zone OL-1 probably reflects a period with moder-ately wet climates since rain forest and peatswamp pollen dominate assemblages. Zone OL-2,

on the other hand, probably reflects a period ofmarginally seasonal climates. The assemblagesthrough OL-2 are in fact mainly dominated byeverwet rain forest climate elements, but theconsistent occurrence of pollen of Poaceae, Schou-tenia and of ‘Australian’ Austrobuxus/Dissiliaria(Malvacipollis diversus) and reduced representationof peat swamp elements suggests that vegetationcharacteristic of more seasonal climates must havehad a distinct presence in the sediment source area.

Within zones OL-3 and OL-4, the dominance ofpollen of ‘Kerapah’ type peat swamp elements,such as Dacrydium and Casuarina type, and the dis-appearance of riparian elements (ecologicallyreplaced by the Kerapah group) suggests a periodof everwet to superwet climates. With the reductionof the Kerapah group in zone OL-5, and return ofriparian elements, a change to a slightly less wet(but still everwet) climatic regime is indicated forthe uppermost interval.

It is because the palynological zones are char-acterized by elements suggesting regional climatechange that the zones are thought to be of potentiallywide correlatable significance.

Fig. 8. Climate sketches for zones OL-2, 3 and 4. superimposed on palaeogeographic maps of Hall 1998. Stipple, landarea; grey shading, shelf; brick pattern, limestone platforms; triangles, volcanoes.

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Discussion

East Java wet climate province

For most of the Oligocene in SE Asia seasonalclimate assemblages are the rule (e.g. Morley2000; Morley et al. 2003; Morley & Shamsuddin2006) although essentially everwet climates haverecently been interpreted for the Udang Formationin Block B, West Natuna (southernmost partof Natuna) by Morley et al. (2007). The wettestclimates recorded for the Oligocene, however, arefrom the Java region and probably reflect a wetclimate fringe to the eastern margin of Sundalandprior to the collision of the Australian and Asianplates at the Oligo-Miocene boundary. The periodof wetter climate approximately coincides withthe Late Oligocene thermal maximum as recordedfrom isotopes by Zachos et al. (2001). Possible

palaeoclimate sketches for zones OL-2, andOL-3/4 are shown in Figure 8.

Correlation to Sunda Basin

Zone OL-2, with regular Malvacipollis diversus,and regular seasonal climate elements, can be cor-related directly to the ‘Freshwater’ Talang Akarand Cibulakan Formations in the Sunda Basin,with zones OL-3 and OL-4 corresponding to the‘Coaly’ Talang Akar (Fig. 9). Zone OL-2 can beaccurately dated using nannofossils to zone NP24(27–29 Ma) and this provides the first direct ageattribution to the Freshwater Talang Akar/Cibula-kan Formations in the Sunda/Arjuna region. TheOL-2 seasonal climate event probably has a widestratigraphic application across the Sunda region,and may correlate to palynological zones PIV–PV

Fig. 9. Correlation to Sunda Basin. See caption to Figure 4 for explanation of pollen groupings.

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(Morley et al. 2003) in Natuna Basin and zonesPR1–4 in the Malay Basin (Azmi et al. 1996).

Occurrence of pollen of Dacrydium

and Casuarina type in the Oligocene

of East Java

This study extends the record of Dacrydium andCasuarina type pollen from the Oligo-Mioceneboundary (Morley 2000) to the base Oligocene, pre-viously brought to attention by Lelono (2007).

Previously, it was thought that these two taxadispersed into the Sunda region following the col-lision of the Australian and Asian plates, at theOligo-Miocene boundary (Morley 1998, 2000),but this study suggests that this is unlikely, sinceat the time of the basal Oligocene, when thesepollen types first appear, the Australian land masswould have been some 1000 km south of the EastJava area. Recently, additional records of Dacry-dium pollen have been reported from the Eoceneof the Indian subcontinent (Morley 2011) and itcan now be proposed that Dacrydium dispersedinto SE Asia prior to the Early Oligocene via theNinetyEast Ridge (where it has been reported fromthe Paleocene by Kemp & Harris (1975) and theIndian Plate (Fig. 10). Its distribution acrossthe Sunda region and Indochina is thought to belimited by palaeoclimate, explaining why it ispresent in some areas of the Sunda region and inthe SE Asian mainland, in the Oligocene of SouthernChina (Sun et al. 1981) and Late Oligocene of

Vietnam (Morley unpublished) characterized bywetter climates, but not other areas where climateswere more seasonal (Morley 2010). A model toexplain the dispersal of Casuarinaceae into theSunda region remains unresolved, since dispersalvia India is unlikely as there is no pollen recordfrom the Indian subcontinent prior to the Miocene.Long distance dispersal may be a possibility.

The authors are grateful to Anadarko Indonesia andMIGAS for permission to publish this paper. The foramini-fera and nannofossils discussed in this paper were ident-ified by biostratigraphers at LEMIGAS. Carlos Jaramilloand Margaret Collinson provided suggestions which haveimproved the manuscript.

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