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Palaeogeography, Palaeoclimatology, Palaeoecology 160 (2000) 123–151www.elsevier.nl/locate/palaeo

Triassic pelagic deposits of Timor: palaeogeographicand sea-level implications

R. Martini a,*, L. Zaninetti a, M. Villeneuve b, J.-J. Cornee b, L. Krystyn c,S. Cirilli d, P. De Wever e, P. Dumitrica e, A. Harsolumakso f

a Dep. de Geologie et Paleontologie, Univ. of Geneva, 13 rue des Maraıchers, 1211 Geneva 4, Switzerlandb CNRS UPRESA 6019, Univ. de Provence, 13331 Marseille Cedex 03, France

c Institute for Paleontology, Univ. of Vienna, 14 Althanstrasse, 1090 Vienna, Austriad Dipartimento di Scienze della Terra, Univ. of Perugia, 4 piazza Universita, 06100 Perugia, Italy

e Laboratoire de Geologie, Museum National d’Histoire Naturelle, 43 rue Buffon, 75005 Paris, Francef Department of Geology, Institute of Technology Bandung (ITB), Jalan Ganesha 10, Bandung 40132, Indonesia

Received 10 December 1998; received in revised form 5 August 1999; accepted for publication 13 January 2000

Abstract

In West Timor, Triassic deposits are found in the Parautochthonous Complex, as well as in the Allochthonousseries of Sonnebait. A detailed biostratigraphic investigation, integrating field observations and facies analysis, allowedthe reconstruction of a synthetic lithostratigraphic succession for the Upper Triassic; a stratigraphic transition fromCarnian shales to Upper Norian–Rhaetian limestones is also shown by this study. The fossil content predominantlyoriginates from an open marine environment; lithostratigraphic Units A–E are dated on the basis of radiolaria andpalynomorphs, and Unit H, on ammonites and conodonts. The presence of pelagic bioclasts, together with normalgrading, horizontal laminations, and current ripples, is indicative of a distal slope to basin environment. The ammoniterich condensed limestone of Unit H was deposited on a ‘pelagic carbonate plateau’ exposed to storms and currents.The organic facies have been used as criteria for biostratigraphy, palaeoenvironmental interpretation, and sequencestratigraphy. The palaeontological analysis of the Triassic succession of West Timor is based on the investigation ofradiolaria and palynomorphs, in the marls and limestones of Units A–E, and also on ammonites and conodonts inthe condensed limestone of Unit H. Units A and B are Carnian (Cordevolian) in age, based on the occurrence of thepalynomorph Camerosporites secatus, associated with ‘Lueckisporites’ cf. singhii, Vallasporites ignacii, Patinosporitesdensus and Partitisporites novimundanus. Unit C is considered as Norian, on the basis of a relatively high percentageof Gliscopollis meyeriana and Granuloperculatipollis rudis. Unit D contains significant palynomorphs and radiolaria;the organic facies, characterized by marine elements, is dominated by the Norian dinocysts Heibergella salebrosaceaand Heibergella aculeata; the radiolaria confirm the Norian age. They range from the lowermost Norian to the lowerUpper Norian. Unit E also contains radiolaria, associated in the upper part with the well-known marker of the UpperNorian, Monotis salinaria. For Unit E, the radiolaria attest to a Lower to Upper Norian age based on the occurrenceof Capnodoce and abundant Capnuchosphaera; the upper part is Upper Norian to Rhaetian based on the presence ofLivarella valida. Finally, the blocks of condensed limestone with ammonites and conodonts of Unit H allowed thereconstruction of a synthetic stratigraphic succession of Upper Carnian to Upper Norian age. Our stratigraphic data

* Corresponding author. Fax: +41-22-320-57-32.E-mail addresses: [email protected] (R. Martini), [email protected] (M. Villeneuve),

[email protected] (L. Krystyn), [email protected] (S. Cirilli), [email protected] (P. De Wever)

0031-0182/00/$ - see front matter © 2000 Elsevier Science B.V. All rights reserved.PII: S0031-0182 ( 00 ) 00062-6

124 R. Martini et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 160 (2000) 123–151

lead to the suggestion that the Allochthonous complex, classically interpreted as a tectonic melange of the accretionaryprism of the Island Arc of Banda, is a tectonically dismembered part of a Triassic lithostratigraphic succession.© 2000 Elsevier Science B.V. All rights reserved.

Keywords: Ammonoidea; Conodonta; palynomorphs; radiolaria; sedimentology; Timor; Triassic

1. Introduction cal complex of Banda (Fig. 1). Two major geody-namic events are identified:

Timor has been considered by previous authors $ the obduction of ophiolitic, metamorphic, andto be part of the Northern Australian margin sedimentary material, known as the(Northeastern Gondwana), during Palaeozoic and Allochthonous complex, on the AustralianEarly Mesozoic times, before the Middle Jurassic margin in the Late Oligocene, or Early Miocenefragmentation and Cretaceous drifting to the (Sopaheluwakan, 1990);North of the Gondwana marginal fragments. $ the collision, in the Lower Pliocene, between

The Permian and Triassic of Timor have long the Australian margin and the volcanic arc ofbeen known because of the abundance and quality Banda (Harsolumakso, 1993; Charlton andof the macrofauna, mostly ammonites, bivalves, and Wall, 1994); this explains the fore-arc positionbrachiopods (Rothpletz, 1892; Wanner, 1907, 1913, of Timor with respect to the island arc of Banda1932; Welter, 1914, 1915, 1922; Haniel, 1915; (Fig. 1).Krumbek, 1921; Diener, 1923; Krumbek, 1924; From a structural point of view, the island ofSmith, 1927; Grunau, 1953; Krystyn and Siblik, Timor is classically subdivided into three tectonic1983; Krystyn and Wiedmann, 1986; Cook et al., complexes (Grunau, 1953; De Ward, 1957;1987; Archbold and Barkham, 1989). Nevertheless, Gageonnet and Lemoine, 1958; Lemoine, 1959;despite the comparatively high number of outcrops, Audley-Charles, 1968; Barber et al., 1977; Rosidithe Triassic deposits of Timor remain poorly et al., 1979; Charlton, 1987; Bird and Cook, 1991;described, at least as far as sedimentology and Harsolumakso, 1993; Sawyer et al., 1993) (Fig. 2):micropaleontology are concerned. This is mostly due

$ The Parautochthonous complex, essentiallyto the tectonic fragmentation of the series, and also

composed of thick sedimentary deposits ofto the monotony of the dominant basinal TriassicPermian to Oligo-Miocene age. This complex,carbonate facies with radiolaria and filaments.referred to the Australian passive margin, isOur geological research since 1990 in therepresented by the Kolbano formationAllochthonous and Parautochthonous complexes(Charlton and Wall, 1994) at the extreme southof Timor allowed the identification and dating ofof the island, the series of Kekneno to the NWthe different Triassic lithological units, especially(Bird and Cook, 1991), and the formations ofthe limestones, and reconstruction of a syntheticthe NE part of the island (Gageonnet andstratigraphic succession. The analysis of theLemoine, 1958).Triassic depositional conditions and fossil content

$ The Allochthonous complex, of unknownis also fundamental for future comparisons withorigin, represented by exotic nappes made ofthe Northeastern Gondwana margin and theJurassic to Oligocene ophiolitic, metamorphicmicrocontinents of East Indonesia, such as theand sedimentary rocks. The series of Sonnebaitrecently defined Banda and Lucipara blocks(or Bobonaro Scaly Clay), composed of(Martini et al., 1997; Villeneuve et al., 1998).Permian to Oligo-Miocene sedimentary forma-tions, are also part of the Allochthonous; theyare classically interpreted as the tectonic2. Geological settingmelange of the accretionary prism of the islandarc of Banda.The island of Timor is the result of a collision

between the Australian continent and the geologi- $ The Autochthonous complex, which consists of

125R. Martini et al. / Palaeogeography, Palaeoclimatology, Palaeoecology 160 (2000) 123–151

Fig. 1. Location map of the Island of Timor in the Volcanic arc of Banda.

Lower Miocene to Recent detritic and volcano- (Rosidi et al., 1979), or in more detail in smallerlocalities, or short stratigraphic intervals (Gageonnetsedimentary deposits, accumulated after the

Oligocene obduction of the Allochthonous and Lemoine, 1958; Audley-Charles, 1968; Kristan-Tollmann et al., 1987; Bird and Cook, 1991). Mostcomplex on the Australian margin. The

Autochthonous is essentially represented in the of the studied series are located in anticlines of theParautochthonous Complex, such as the Cribascentral basin of Timor.Mountain in Eastern Timor (Gageonnet andLemoine, 1958), or the Kekneno (Cook et al., 1987)and Kolbano Mountains (Charlton, 1987; Charlton3. Triassic in West Timorand Wall, 1994), to the SW.

In the so-called tectonic melange of theTriassic deposits are found in theParautochthonous complex, as well as in the Allochthonous (Sonnebait series), the geological

data concerning the Triassic are far less abundant.Allochthonous series of Sonnebait. The facies ofthe two series are monotonous: they are of the Rosidi et al. (1979) restudied the Triassic while

establishing the geological map of West Timor toflysch type in the Parautochthonous complex, andcalcareous in the Allochthonous, pelagic in origin the 1:250 000 scale. Charlton (1987) studied in

detail five small areas close to the south coast ofwith radiolaria and filaments. CharacteristicTriassic radiolaritic limestones and nodular lime- the island, while Harsolumakso et al. (1995)

improved the stratigraphy of the Sonnebait series;stones are very common in tectonic subunits orscales, as described below. They can be used as the area was also investigated by Sawyer et al.

(1993) for oil companies. From a lithostrati-indicator levels for the Allochthonous.In West Timor, the series containing Triassic graphic point of view, Kristan-Tollmann et al.

(1987) noted similarities of the allochthonoussediments have been studied throughout large areas


Fig. 2. Main structural and geological units of Timor (after Audley-Charles, 1968; Harsolumakso, 1993), and location maps of theA–B cross-sections in the studied area (Noe Fatu, Noe Meto, and Noe Bihati).

Upper Triassic series in Central Timor with coeval Nikiniki area, Noe Meto near Soe, and Noe Bihatiin the Baun area near Kupang (Fig. 2).classic formations of Hallstatt facies in the

Eastern Alps. Nevertheless, a detailed Triassic Lithostratigraphic Units, named A–E, and H, havebeen identified and dated. Units A–E are repre-sequence from the Carnian to the Upper Norian,

as well as the transition from the Carnian shales sented in a complete succession in the localitiesNoe Fatu and Noe Meto. They exhibit a similarto the Upper Norian–Rhaetian limestones with

radiolaria, do not seem to have been recognized lithology, and can be identified only on the basisof their microfossil content (radiolaria and palyno-before this study.morphs). Unit H, only recorded in the Noe Bihatiarea, looks quite different; it is composed of ahighly fossiliferous condensed limestone with4. Lithostratigraphy and sedimentologyammonites and conodonts (Hallstatt facies).

Isolated samples, collected in the localities NoeThe sedimentological analysis of the UpperTriassic of West Timor is based on the study of Tobe, Fatununu, and Noe Teknono, are integrated

in the litho- and biostratigraphic description, onthree major geological sections, all located in theAllochthonous series of Sonnebait (or Bobonaro the basis of facies similarities with the main Triassic

fossiliferous lithotypes of West Timor.Scaly Clay). The sections are Noe Fatu in the


Fig

.3.

Det

aile

dge

olog

ical

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ions

ofN

oeM

eto,

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Bih

ati,

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Noe

Fat

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4.1. Noe Fatu section section is subdivided into three superimposed tec-tonic subunits or scales (S1, S2, S3) (Fig. 3). Acomplete lithostratigraphic succession of Units A–The most representative Triassic section of West

Timor is exposed along the Fatu River (Noe Fatu), E is found only in the lowermost scale S1. Themiddle scale S2, which shows a strongly foldedEast of Nikiniki (Fig. 2.1). Noe Fatu is a medium-

sized river, about 30 m in width, oriented NNW– structure to the North, extends on lithostrati-graphic Units B–E. The upper scale S3 is entirelySSE in the studied area; the river bed is dominantly

dry, except during the monsoon period (March– composed of lithostratigraphic Unit A.A detailed biostratigraphic analysis of the scalesMay).

The geological section is located at the shoal of allowed the reconstruction of a synthetic litho-stratigraphic succession for the Upper Triassic ofthe Nikiniki–Oinlasi road; it covers the interval

from the Triassic (upstream) to the Cretaceous West Timor, essentially based on the Noe Fatusection (Fig. 4). Because of the dominant basinal(downstream). Several authors (Harsolumakso,

1993; Sawyer et al., 1993; Harsolumakso et al., Triassic facies with radiolaria and filaments, thiswas possible only by integrating field observations1995) showed that the series of Noe Fatu corre-

spond to a lithostratigraphic succession, tectoni- and micropaleontological data.cally dismembered, and so they cannot beconsidered as part of the olistostrome of the accre- 4.1.1. Description of the lithostratigraphic units

Lithostratigraphic Units A–E are made of claytionary prism of Timor. Our results tend to confirmthis interpretation, as it was possible to demon- and limestone, characterized by thin shelled

bivalves (filaments) and radiolaria, originatingstrate that the Triassic interval of the Noe Fatu

Fig. 4. Synthetic stratigraphic successions of the Upper Triassic sedimentary rocks in the West Timor (Noe Fatu, Noe Meto, andNoe Bihati), with productive samples and age diagnostic organisms. Noe Bihati: the succession is restarted (1) from continuousoutcrops, (2) from isolated blocks.


from an open marine pelagic environment (Fig. 5). nized. A decimetre-scale level of black peat, richin pyritic nodules (up to 3 cm), occurs 2 m fromRare shallow platform bioclasts (benthic foramini-the base of the unit. Mudstone and wackestonefers, remnants of bivalves, ostracods and echino-are the dominant microfacies of the micriticderms) have been observed in a few samples.limestone; the nodular limestone is charac-Turbidity currents, evidenced by the bioclasts, asterized by a radiolarian packstone, either lami-well as by sedimentary structures (e.g. normalnated or homogenized due to bioturbation. Thegrading, horizontal lamination, as well as smallage, based on radiolaria assemblages and paly-current ripples), are indicative of a more or lessnomorphs, is Norian.distal slope to basin environment. Nodular lime-

Unit E. Eighteen metres of centimetre- to decime-stone, only observed at the top of Unit D, Noetre-scale levels of white–grey micritic limestoneFatu section, is the result of early diagenetic pres-with radiolaria; grey to red marls form verysure dissolution.thin interbeds. Remarkable accumulations ofThe lithostratigraphic Units A–E are, fromMonotis salinaria (as filaments) characterize thisbottom to top (Fig. 4):unit, as well as chert nodules, and siliceous

Unit A. About 10 m of black well-stratified clays levels, derived from radiolarian tests. The char-acteristic texture type is wackestone/packstone,and marly clays, with small ferrugineous nod-in which the micritic groundmass containsules and sulphur pseudomorphs; the clays con-abundant filament coquinas. M. salinaria is atain a significant palynological assemblage,well-known marker of the Upper Norian; thisindicative of a Carnian age.interval is confirmed by the radiolaria assem-Unit B. Four metres of satin-like grey to blackblages, which attest to an Upper Norian towell-stratified clays and marly clays, alternatingRhaetian age.with centimetre-scale interbeds of greenish,

sometimes radiolaritic, limestone with filaments;the dominant microfacies is a bioclastic pack-

4.2. Noe Meto Sectionstone. The lowermost Carnian (Cordevolian)age of Unit B is based on palynological data.

The Meto river (Noe Meto) flows in a largeUnit C. Three metres of decimetre scale beds ofalluvial plain, located in the area south of Soe.red variegated bioclastic (radiolaria and fila-The studied geological section extends in a NE–ments) limestone, alternating with centimetre-SW portion of the river, upstream from the tribu-scale levels of black to red marls; radiolaria aretary Noe Kele (Fig. 2.2). The same lithostrati-

sometimes visible on the bed surfaces.graphic units as identified in the Noe Fatu section

Packstone, rarely grainstone, is the most fre- are recognized (Fig. 3): Unit A, with a S–SE low-quent microfacies. Because of the poor preserva- grade regional dip; Units B and C (only smalltion, radiolaria could not be used for portions); Units D and E. Because the topographybiostratigraphy; the palynological content indi- is practically constant, the outcrops hardly risecates a Norian age. above the river bed. In addition to this unfavoura-

Unit D. Seventeen metres of decimetre-scale beds ble situation, the formations are moreover tectoni-of white micritic limestone, sometimes with red cally repeated. For these reasons, the syntheticsparks, characterized by filaments and rare stratigraphic section for the Triassic of Noe Metoradiolaria; towards the top, the beds become has been mainly reconstructed on the basis ofthicker, richer in radiolaria, and alternate with micropaleontological data (Fig. 4). Due to discon-grey marls. The top itself is composed of white tinuous exposure conditions, Units A–E could notnodular limestone with millimetre-scale marly be measured; their thickness is based on that ofinterbeds. On the bed surfaces, the brachiopod the Noe Fatu section.Halorella pedata Bronn, and the bivalve The lithotypes, cropping out along the Noe

Meto, have been preliminarily studied by Kristan-Monotis salinaria (SCHLOTHEIM) are recog-


Fig. 5. Depositional model of the Upper Triassic series of West Timor.

Tollmann et al. (1987); the authors noticed similar 4.3. Noe Bihati sectionfacies to those from ‘‘formations of the classicEastalpine Upper Triassic–Liassic stages in The Bihati torrent (Noe Bihati) flows east ofHallstatt facies’’. Baun, 20 km SE of Kupang, the chief town of

West Timor.The studied section, located along a W–E por-

tion of the river (Fig. 2.3), reflects the geologicalcomplexity of the area, with Tertiary series intectonic contact with Triassic radiolaritic lime-stones. In fact, on the right bank of Noe Bihati,limestones with Nummulites are observed, as wellas peridotites blocks, which recall the exotic nappesof Timor (Fig. 2); on the left bank, Triassic depos-its are exposed.

Lithostratigraphic Units B–E, already identifiedin the Noe Fatu and Noe Meto sections, are alsorecognized in the Noe Bihati area; they can beobserved in a Triassic syncline (Fig. 3); Unit A ismissing in the studied section.

An additional lithostratigraphic unit ( Unit H,after Hallstatt) for the Noe Bihati area, notrecorded in the Noe Fatu and Noe Meto sections,is represented by white to pink highly fossiliferous(ammonites) condensed limestone of Hallstatttype. The tectonically dismembered unit is reducedto isolated blocks of variable size (maximum6 m3).

A synthetic stratigraphic succession, based onUpper Triassic microfossils, and on the ammonitesFig. 6. (A) Sequence stratigraphy interpretation of the Upperof the boulders, has been reconstructed for litho-Triassic basinal carbonate sequence of West Timor and (B)

correlation with the cycle chart of Haq et al. (1987). stratigraphic Units B–E, and H (Fig. 4). These


units are capped, in the area of Noe Bihati, by H2. Condensed pink–red micritic limestone, withblack argilites with manganese and sulphur pseu- ammonites (60% matrix; 40% fossils). The lime-domorphs that look similar to those of lithostrati- stone is predominantly composed of completegraphic Unit A, in the Triassic Noe Fatu and Noe specimens of ammonites and characterized byMeto sections. According to Sawyer et al. (1993), a high percentage of stylolites. The ammonitesthe argilites of Noe Bihati are of Liassic age. are represented only as casts, and they are often

eroded. The fossils are arranged parallel to thestylolitic joints.

4.3.1. Lithostratigraphic Unit H Unit H is interpreted as being deposited on aDue to its rich ammonite fauna, the Noe Bihati ‘pelagic carbonate plateau’ (or sea mount),

area has been investigated since the 1970s by located below the depth favourable for reefseveral authors (Tatzreiter, 1978; Krystyn and growth (Fig. 5). The ‘pelagic carbonate pla-Siblik, 1983; Krystyn and Wiedmann, 1986; Baud teaus’ are known to be exposed to storms andand Marcoux, 1991). According to these authors, currents, responsible for a discontinuous deposi-the boulders are part of a large olistostrome, tional sequence, interrupted by intervals ofprobably younger than Tertiary (Pleistocene), omission due to erosion, or to reduced sedi-today dismembered and scattered in a large part mentation rate (0.1–1 mm/Ma, according toof Timor. Older studies (e.g. von Bemmelen, 1949; Einsele, 1992). Irregular bedding and nodularGageonnet and Lemoine, 1958) used to classify structures are common, as well as hardgroundsthis tectonic block complex (melange) as an alpine with ferromanganese nodules, and spectaculartype under the name of Fatu-Klippen; the age of accumulations of cephalopods; also characteris-the blocks is Upper Palaeozoic (reefal limestone) tic is the red colour. Except for the absence ofto Eocene (Nummulitic limestone). polymetallic nodules, but in the presence of

During our field trip in Timor in 1993, the polymetallic coatings around the megafossils,blocks of lithostratigraphic Unit H were sampled this description is adequate for the fossiliferousin detail, as the Bihati river was free of water at limestone of Unit H. Such deposits of the Rossothat time of the year (September). This was appa- Ammonitico type are common in the geologicalrently not the case for the previous geological record; they were described from the Triassicmissions in the Baun area, reported in the (Hallstatt limestone) and from the Jurassic andliterature. Cretaceous of many regions of the Tethyan

Two different lithologies are recognized in Realm ( Krystyn, 1973; Bernoulli and Jenkyns,Unit H: 1974; Fursich, 1979; Krystyn, 1980; Jenkyns,

1986).H1. Condensed fossiliferous white–pink limestone(10% micritic matrix, 90% fossils). The organ-isms are mostly represented by cephalopods(ammonites and nautiloids), sometimes large(60 cm) and often broken; brachiopods,

5. Organic faciesbivalves, gastropods, and echinoderms are alsofound. The pelagic hydrozoan Heterastridium is

Palynological analysis has been carried out inalso quite common. In this facies, the shells areargillaceous and marly intervals from the Noeremarkably preserved, and they normallyFatu, Noe Meto and Noe Bihati Triassic sections;exhibit a black patina; this colour is due toonly lithostratigraphic Units A–D provided pro-polymetallic coatings, linked to the anoxic con-ductive results. The organic compounds have beenditions of the depositional environment. As agrouped according to Whitaker’s classificationrule, the blocks are poorly compacted, a situa-(Whitaker, 1984), and the palynofacies used astion that allows, together with the scarcity of

the matrix, the easy extraction of the fossils. criteria for palaeoenvironmental interpretations


(Tyson, 1987, 1993, 1995; Huc, 1988; Steffen and reduced; only a low percentage of vitrinite(PM2+PM3) and of small equidimensional iner-Gorin, 1993).tinite (PM4) is observed. Palynomorphs areabsent, as well as AOM.

Unit A

Unit CBlack, well-stratified clays and marly clays(TM36, Noe Fatu) have been processed to study

The organic facies has been obtained from blackthe organic facies. This is characterized by a largeto red marls alternating with the dominant bioclas-amount of amorphous organic matter (AOM), atic limestone of Unit C (TM41, Noe Meto); it islow percentage of vitrinite (PM1+PM2) andcharacterized by a high percentage of unsortedmostly bladed inertinite (PM4T). This organicvitrinite (PM1+PM2) and equidimensional iner-facies appears devoid of heavy ornamented spores.tinite (PM4); wood remains are common, withThe sporomorph content, with a predominance offungal remains; AOM is absent. Palynomorphssaccate specimens, is moderately high, while therepresent about 30% of the organic facies, mostlypercentage of marine elements, such as theconsisting of ornamented spores and circumpol-Prasinophyte alga Tasmanites and chitinous fora-lens, rather than bisaccates.miniferal linings, is even more conspicuous. The

association of prasinophyte algae and finely lami-nated sediments is typical of many Palaeozoic and Unit DJurassic black shale facies (Tyson, 1995).

The organic facies of the grey marls, alternatingwith micritic limestone containing filaments andUnit Bradiolaria (TM35, Noe Fatu; TM55, NoeTeoknono), is dominated by small equidimensionalThe organic facies has been obtained from satin-inertinite particles (PM4, about 60%), which arelike grey to black clays and marly clays of themedium rounded and well sorted; vitrinitelower to middle portion of the unit (TM6, Noe(PM1+PM2) is present in minor amounts ( lessFatu; TM51, Fatu Nunu); it is characterized by athan 5%). Among palynomorphs, marine elementshigh percentage of large vitrinite (PM1+PM2),are dominant, largely represented by dinocysts.mostly consisting of wood remains; the percentageLess abundant are the sporomorphs, commonlyslightly increases from the base up to the middlerepresented by smooth spores and small bisaccates.portion, ranging from about 30 to 50%. A lowerA small amount of degraded AOM is present.percentage of small size equidimensional inertinite

(PM4) is observed, from 10 to 20% in the middleportion. Palynomorphs represent about 40–50% 5.1. Palaeoenvironmental interpretationof the organic facies, with a great variety in numberand species of saccate sporomorphs (monosaccates Marine organic-rich laminated sediments pro-

duced the organic facies of Unit A; because of theand bisaccates). Large, heavily ornamented sporesare very common, as well as bisaccates; their high ratio of marine/terrestrial elements and

bisaccate/heavy ornamented spores, the abundancerelative proportion slightly decreases upwards con-comitant with the increase of vitrinite. AOM is of AOM, and the abundance of bladed inertinite

on other palynomacerals (PM1+PM2), this typeabsent. The ratio of terrestrial elements vs. marineelements is high, the latter being represented only of organic facies is considered of distal origin,

deposited under dysoxic–anoxic conditions. Beingby few acritarchs. This palynofacies is charac-terized by the predominance of land-plant remains the AOM the more labile elements among the

organic compounds, its preservation is possible(vascular tissue facies, sensu Habib and Miller,1989). In the upper portion of the unit (TM20, only in low oxygenated waters. It is also supported

by the dominance of Prasinophyte algaeNoe Fatu), the total amount of OM is drastically


(Tasmanites), which are considered as ‘disaster tive of a general initial trend in offshore direction(Tyson, 1993, 1995). Distal conditions are alsoforms’ (Tappan, 1980), capable of surviving under

stressed conditions; their abundance in distal facies suggested by the presence of smooth spores andsmall bisaccates, which are the most easily trans-is also considered as typical of ‘condensed sections’

within a transgressive system tract or an early ported and most buoyant of all sporomorphs.Also, large amounts of equidimensional inertinitehighstand system tract (Loutit et al., 1988; Leckie

et al. 1990; Tyson, 1995). in Unit D provide the same indication, as thisresistant palynomaceral can be transported farThe organic facies of Unit B revealed a deposi-

tional environment corresponding to a nearshore away from the source area.The occurrence of this palynofacies within ashallow shelf within a progradation phase. It is

indicated by the predominance of land plant micritic limestone containing filaments andradiolaria suggests the beginning of a highstand,remains together with a high percentage of orna-

mented sporomorphs and inertinite, together with with a subsequent trapping of most of the terrige-nous material on the shallower shelf, and thebisaccates and heavily ornamented spores. The

same indication is given by the large particles of conquest by dinocysts of new ecological niches.Organic facies of Unit C and D reveal a trans-vitrinite, with the distribution of the phytoclasts

being strongly affected by the granulometric com- gressive trend, whose Unit C can be related to thebeginning of a new phase of relative sea-level rise.position of the sediment and by hydrodynamic

selection.Within the regressive trend of Unit B, the

inertinite facies that is dominant in the upper part6. Biostratigraphy

appears to be representative of the top of theregression phase. The predominance of inertinite

The biostratigraphic evaluation is based on thedue not to its absolute increase, but mostly to the

investigations of radiolaria and palynomorphs inabsence of other organic particles, indicates that

the marls and micritic–bioclastic sometimes nodu-the OM was strongly affected by destructive phys-

lar limestones of Units A–E, and also of ammonitesico-chemical processes such as oxidation and

and conodonts from the condensed limestone ofstrong bioturbation. In such oxygenated condi-

Unit H.tions, inertinite, which is more or less chemicallyinert, remains the dominant type of OM.

6.1. RadiolariaIn Unit C, the relative abundance of spores, thepresence of fungal hyphens, and the abundance of

Lithostratigraphic Units B–E contain radiola-total recycled material (palynomacerals plus spor-ria; they are normally present in the greenishomorphs) are still indicative of the proximity tobioclastic limestone of Unit B, in the red variegatedthe land. The absence of AOM can be explainedbioclastic limestone of Unit C, in the white micriticby oxic depositional conditions, unfavourable tosometimes nodular limestone of Unit D, and inthe preservation of this type of labile OM. Thethe white–grey micritic limestone of Unit E.high degree of preservation of particulate OMNevertheless, the extraction of radiolaria was pos-could be related to a relatively high sedimentationsible only in Units D and E because of theirrate that reduces the effects of the oxidation onpreserved original siliceous tests (Plates I and II ).OM. In fact, under such conditions, OM is quickly

removed from the water–sediment interface, whereit would be easily oxidized. Unit D

Unit C overlies dominant marine organic faciesof Unit D. This palynofacies is referable to a distal This lithostratigraphic unit is represented by

micritic limestone with filaments and radiolaria,mud-dominated oxic shelf (sensu Tyson, 1993),removed from active sporomorph input. alternating towards the top with grey marls; four

samples, from the Noe Fatu, Noe Meto and NoeThe high dinocyst/sporomorph ratio is indica-


PLATE I

1, 2. Capnuchosphaera sp., inner cast. Sample TM 77, Noe Bihati.1. General view.2. Detail of a spine. The shell being dissolved displays the inner structure of the sphere and, more interestingly, the structure

of the spines. It is clear that the proximal part is an hollow tube, while the distal part is divided into three longitudinal partsby lamellae. Upper Carnian?–Lowermost Norian.

3 Capnuchosphaera aff. lea De Wever. Sample TM77, Noe Bihati. Upper Carnian?–Lowermost Norian.4. Capnuchosphaera theloides De Wever. Sample TM77, Noe Bihati. Upper Carnian?–Lowermost Norian.5. Capnuchosphaera tricornis De Wever. Sample TM37, Noe Meto. Lower to Middle Norian.6. Betraccium sp. Sample TM38, Noe Meto. Upper Middle Norian–Lower Upper Norian.7. Capnuchosphaera triassica De Wever. Sample TM77, Noe Bihati. Upper Carnian?–Lowermost Norian.8. Capnuchosphaera anapetes De Wever. Sample TM37, Noe Meto. Lower to Middle Norian.9, 11. Spumellaire gen. sp. indet. Sample TM38, Noe Meto. Upper Middle Norian–Lower Upper Norian.10. Capnuchosphaera triassica var. a De Wever. Sample TM37, Noe Meto. Lower to Middle Norian. Scale bar: 50 mm.


PLATE II

1, 2. Livarella valida Yoshida 1986. Sample TM33, Noe Fatu. Rhaetian or Upper Norian to Rhaetian.3. Paronaella norica Kozur and Mock. Sample TM37, Noe Meto. Lower to Middle Norian.4. Gorgansium beaverense Yeh. Sample TM38, Noe Meto. Upper Middle Norian–Lower Upper Norian.5. Praemesosaturnalis finchi (Pessagno). Sample TM38, Noe Meto. Upper Middle Norian–Lower Upper Norian.6. Corum regium, Blome. Sample TM37, Noe Meto. Lower to Middle Norian.7. Syringocapsa batodes De Wever. Sample TM37, Noe Meto. Lower to Middle Norian.8. Poulpus cf. transitus Kozur and Mostler. Sample TM38, Noe Meto. Upper Middle Norian–Lower Upper Norian.9. Praeorbiculliformella cf. vulgaris Kozur and Mostler. Sample TM77, Noe Bihati. Upper Carnian?–Lowermost Norian.10. Gen. sp. indet. Sample TM37, Noe Meto. Lower to Middle Norian. Scale bar: 50 mm.


Biahti sections, and from locality Noe Teknono, De Wever in De Wever et al. (1979), C. triassicaDe Wever var. A in De Wever et al. (1979),provide productive results.

In Noe Fatu, only a few specimens of saturnal- Capnodoce anapetes De Wever in De Wever et al.(1979), Betraccium smithi Pessagno in Pessagnoids were found in the lower part of Unit D (sample

TM9, TM10); the species Palaeosaturnalis cf. quad- et al. (1979), Betraccium? sp., Astrocentrus cf.pulcher Kozur and Mostler (1979),riradiatus ( Kozur and Mostler, 1972) is indicative

of a Carnian–Norian age. Hungarosaturnalis sp., and other Spumellariansgen. sp. indet., Corum parvum Yeh (1989),In Noe Meto, a very rich sample comes from

the middle part of Unit D (TM38); the following Canoptum cf. macoenses Blome (1984), Poulpuspiabyx De Wever in De Wever et al. (1979),species were recognized: Gorgansium beaverense

Yeh (1989), Betraccium sp., Praemesosaturnalis Poulpus sp., and Nassellarians gen. sp. indet.,probably similar to ‘unnamed Nassellaria’ offinchi Pessagno in Pessagno et al. (1979),

Spongostylus aff. carnicus Kozur and Mostler Pessagno et al. (1979), (pl. 5, fig. 7).Sample TM54, which contains the genera(1981), Kahlerosphaera? aff. aspinosa Kozur and

Mock in Kozur and Mostler (1981), Paronaella? Capnodoce and Capnuchosphaera, is assigned tothe Capnodoce Zone of Pessagno et al. (1979),sp., Poulpus cf. transitus Kozur and Mostler

(1981), Triassocampe sp., associated with some emend. Blome (1984), which corresponds to theUpper Carnian?–Middle Norian; nevertheless,unidentifiable Spumellarians.

Although many species could not be deter- according to the general composition of the assem-blage, the probable age of sample TM54 is Lowermined, the occurrence of the pantanellid

Betraccium sp. and Gorgansium beaverense, and Norian to Lower Middle Norian;In Noe Bihati, the productive sample (TM77)the absence of the genera Capnuchosphaera,

Capnodoce, and Livarella, allow the stratigraphic comes from the base of Unit D. It containsKahlerosphaera norica Kozur and Mostler (1981),interval of sample TM38 to be defined with suffi-

cient precision: the genus Gorgansium ranges from Capnuchosphaera constricta ( Kozur and Mostler,1981), described under the name of Sulovella con-the Upper Carnian?–Norian to the Upper Jurassic,

or even to the Lower Cretaceous; the genus stricta Kozur and Mock in Kozur and Mostler(1981), Capnuchosphaera aff. lea De Wever in DeBetraccium is restricted to the Middle Norian to

Rhaetian, while Capnuchosphaera and Capnodoce Wever et al. (1979), Capnuchosphaera theloides DeWever, Capnuchosphaera triassica De Wever,range from the Upper Carnian to the Lower

Middle Norian, and Livarella makes its first Capnuchosphaera sp., with several very interestinginner casts, showing the structure of the spines asappearance in the Upper Norian. Therefore, it is

tentatively proposed that sample TM38 be illustrated in De Wever et al. (1979),Praeorbiculiforma cf. vulgaris Kozur and Mostlerassigned to the interval between the last occurrence

of Capnuchosphaera and Capnodoce, and the (1978), Annulotriassocampe sp., and Poulpus sp.The occurrence of Capnuchosphaera in thisappearance of Livarella. This interval corresponds

to the upper part of the Middle Norian or to the assemblage, as well as the absence of Capnodoceand Betraccium, suggest an Upper Carnian?–lower part of the Upper Norian.

In the Noe Teknono area, near Noe Fatu, an lowermost Norian age.isolated sample (TM54) has been collected. Onthe basis of facies similarities with the main fossilif- Unit Eerous lithotype (micritic limestone with filamentsand radiolaria) of the Triassic series, this sample Only two of the processed samples from grey

to red very thin marly intervals of lithostrati-is assigned to Unit D. The relatively rich and well-diversified radiolarian assemblage is composed of graphic unit E yielded radiolaria.

Sample TM37 comes from the lower part ofParonaella cf. claviformis Kozur and Mostler(1978), Capnuchosphaera theloides De Wever in Unit E, in the Noe Meto section. The assemblage

is unusually rich in Capnuchosphaerids, withDe Wever et al. (1979), Capnuchosphaera triassica


Capnuchosphaera anapetes De Wever in De Wever 6.2. Palynomorphset al. (1979), Capnuchosphaera lea De Wever,Capnuchosphaera tricornis De Wever in De Wever The aim was to support stratigraphic and sedi-

mentological investigations by the observation ofet al. (1979), Capnuchosphaera aff. extenta Blome(1984), Capnuchosphaera theloides De Wever, organic facies. A semi-quantitative study on

organic matter content has been carried out onCapnuchosphaera aff. theloides De Wever similarform illustrated by Yeh, 1990, from the Busuanga several samples of clays and marly clays of litho-

stratigraphic Units A–E. All the investigated strataIsland, pl. 3 fig. 12), Capnuchosphaera triassica DeWever, var. A, and Capnuchosphaera sp. resulted rich in organic matter, but only Units A–

D yielded biostratigraphically significant palyno-Spumellarian gen. sp. indet., Capnodoce antiquaBlome (1983), Nassellarians gen. sp. indet. (some- logical assemblages (Plate III; Table 1).how similar to the ‘unnamed Nassellaria’ ofPessagno et al. (1979) (pl. 4), Canesium sp.,

Unit ASyringocapsa batodes De Wever in De Wever et al.(1979), Paronaella norica Kozur and Mock in

The most representative and dominant speciesKozur and Mostler (1981), Annulotriassocampe?

found in black, well-stratified clays and marly clayssp., Corum regium Blome (1984), and Corum sp.

are Camerosporites secatus, Patinasporites densus,are also part of the association.

Vallasporites ignacii, and Partitisporites novimunda-On the basis of the occurrence of Capnodoce

nus morphon.and abundant Capnuchosphaera, sample TM37 is

Among bisaccates, Staurosaccites quadrifidus,considered to be Early to Middle Norian in age.

Cuneatisporites radialis, Triadispora suspecta,It belongs to the Capnodoce Zone of Pessagno

Triadispora sp., and Angustisulcites grandis areet al. (1979), emend. Blome (1984), which corres-

recognized, as well as rare specimens of Ovalipollisponds to the Upper Carnian?–Middle Norian.

pseudoalatus.Sample TM33 was collected in the upper part

Marine elements are abundantly represented byof Unit E, Noe Fatu section; it contains a relatively

prasinophyte algae (Tasmanites sp.), and foramini-rich radiolarian microfauna. General groups

fera linings.(Nassellarians, Spumellarians) and some families

This palynological assemblage is generically ref-(Pantanellids gen. sp. indet.) have been recognized,

erable to the Camerosporites secatus phase. Thisas well as specific elements: spines of uncertain

phase, based by Visscher and Krystyn (1978) onSpongopallium Dumitrica et al. (1980),

Schuurman (1977, 1979) Phase I, has generallyParatriassoastrum aff. cordevolicum Kozur and

been considered as an event ranging from theMostler (1981), P. aff. crassum Carter (1993) (=

Ladinian to Carnian (Visscher and Brugmann,‘Spumellarian gen. sp. indet. C’ in Yeh (1989),

1981; Van der Eem, 1983; Fisher and Dunay,Paronaella? sp., Betraccium maclearni Pessagno

1984). For the assemblage of Unit A, an essentiallyand Blome (1980), Betraccium sp., Pantanellium

Carnian trend is supported by the combined occur-cf. fosteri Pessagno and Blome (1980), Latium

rences of C. secatus with Vallasporites ignacii,mundum Blome (1984) (=‘Dictyomitra sp. gr.’ in

Patinasporites densus, and Partitisporites novimun-De Wever et al., 1979, pl.5, fig. 14), and Livarella

danus. The presence of P. densus and V. ignaciivalida Yoshida (1986).

suggests that this association may be referred toOn the basis of the occurrence of Livarella

the vigens-densus phase (Cordevolian) of Van dervalida, the age of sample TM33, and consequently

Eem (1983).of the upper part of Unit E, is Rhaetian or UpperNorian to Rhaetian. Some of the species found inthis assemblage were also illustrated by Carter Unit B(1993) from the uppermost Triassic (Rhaetian)radiolarian rich deposits of Queen Charlotte The organic facies of the satin-like grey to black

clays and marly clays of Unit B contains a greaterIslands, British Columbia.


PLATE III


variety of palynomorphs (see Table 1). The most Unit A. The vigens-densus phase is characterizedby the first appearance of P. densus and V. ignacii,representative species are Enzonalasporites vigens,and by the first appearance of Lagenella martinii,Partitisporites novimundanus morphon, common towhich is not present in this assemblage. The speciesall the productive samples; Vallasporites ignacii‘Lueckisporites’ singhii, also characteristic of thisand ‘Lueckisporites’ cf. singhii are abundant inphase, first appears in the older secatus-vigenslevel TM6. Other important elements arephase of Longobardian age; it disappears towardsPatinasporites densus and Camerosporites secatus,the end of the vigens-densus phase; its presence incommon at level TM51. Significant accessory paly-our assemblage strongly supports a lower Carniannomorphs are Calamospora mesozoica,(Cordevolian) age for Unit B.Neoraistrikia taylorii, Cycadopites follicularis,

Deltoidospora spp., Verrucosisporites morulae,Aratrisporites spp., Gordonispora fossulata, Unit CDuplicisporites granulatus, Uvaesporites gadensis,Osmundacites wellmani, Guttatisporites elegans, The organic facies of the black to red marls ofVerrucosisporites applanatus, Ephedripites primus, Unit C contains a relatively high percentage ofand rare Concentricisporites insignis. Gliscopollis meyeriana, Calamospora mesozoica,

Bisaccates are abundantly represented by vari- Concavisporites toralis, Todisporites spp., andous elements. Besides the already cited Cycadopites follicularis. More rare, but strati-‘Lueckisporites’ cf. singhii, the most common are graphically significant, are GranuloperculatipollisLunatisporites acutus, Falcisporites stabilis, rudis, Patinasporites densus, MicroreticulatisporitesAlisporites spp., Angustisulcites grandis, fuscus, and Partitisporites novimundanus morphon.Angustisulcites sp., and Triadispora complex. Rare Gliscopollis meyeriana and Granulo-marine elements occur, and they belong to the perculatipollis rudis are commonly considered asAcritarch genera Micrhystridium sp. and representative of phase II and phase III, of NorianBaltisphaeridium sp. to lowermost Rhaetian age (Morbey and Neves,

The miospore assemblage is indicative of a 1974; Morbey, 1975, 1978; Schuurmann, 1977,Carnian age. The presence of some index taxa 1979; Visscher et al., 1980; Visscher and Brugman,such as Enzonalasporites vigens and Patinasporites 1981; Warrington, 1996). Phase II is characterizeddensus, together with Vallasporites ignacii and by the gradual disappearance of the index species‘Lueckisporites’ cf. singhii, is representative of the of the underlying phase I and by the appearancevigens-densus phase (Van der Eem, 1983), suggest- of characteristic species of the succeeding phases.

The association of the Carnian to Norianing the same Cordevolian age for Unit B as for

PLATE III

1. Camerosporites secatus Leschik 1956. Sample TM36, Noe Fatu. Carnian.2. Patinasporites densus Leschik 1956. Sample TM36. Noe Fatu. Carnian.3, 10. Vallasporites ignacii Leschik 1956. Sample TM36, Noe Fatu. Carnian; Sample TM51, Noe Fatu Lowermost Carnian.4. Ephedripites primus Klaus 1963. Sample TM6, Noe Fatu. Lowermost Carnian.5. ‘Lueckisporites’ cf. singhii Balme 1970. Sample TM6, Noe Fatu. Lowermost Carnian.6. Staurosaccites quadrifidus Dolby in Dolby and Balme 1976. Sample TM6, Noe Fatu. Lowermost Carnian.7. Patinasporites densus Leschik 1956. Sample TM6, Noe Fatu. Lowermost Carnian.8. Concavisporites crassexinius Nilsson 1958. Sample TM41, Noe Meto. Lower to Middle Norian.9. Enzonalasporites vigens Leschik 1956. Sample TM51, Noe Fatu. Lowermost Carnian.11. Partitisporites novimundanus morphon Van der Eem 1983. Sample TM6, Noe Fatu. Lowermost Carnian.12. Gliscopollis meyeriana ( Klaus) Venkatachala 1966. Sample TM41, Noe Meto. Lower to Middle Norian.13. Heibergella salebrosacea Bujak and Fisher 1976. Sample TM55, Noe Fatu, Norian.14. Baltisphaeridium sp. Sample TM6, Noe Fatu. Lowermost Carnian. Graphic scale is 30 microns.


Table 1 Table 1 (continued )Species list of Upper Triassic palynomorphs from Units A–D

Ephedripites primus Klaus 1963Falcisporites stabilis Balme 1970Unit AGordonispora fossulata Van der Eem 1983Significant elementsGuttatisporites elegans Visscher 1966Camerosporites secatus Leschik 1956Illinites sp.Partitisporites novimundanus morphon Van der Eem 1983Infernopollenites parvus Scheuring 1970Patinasporites densus Leschik 1956Infernopollenites sulcatus (Pautsch) Scheuring 1970Vallasporites ignacii Leschik 1956Klausipollenites schaubergeri (Potonie and Klaus) JansoniusTasmanites sp.a1962Foraminifera liningsaKlausipollenites sp.Accessory elementsKrauselisporites dentatus Leschik in Krausel and Leschik 1956Angustisulcites grandis (Freudenthal ) Visscher 1966Krauselisporites sp.Aulisporites astigmosus (Leschik in Krausel and Leschik 1956)Leptolepidites sp.Klaus 1960Lunatisporites acutus Leschik in Krausel and Leschik 1956Cuneatisporites radialis Leschik 1956Microreticulatisporites parviretis Balme 1957Cycadopites follicularis Wilson and Webster 1946Neoraistrikia taylorii Playford and Dettmann 1965Ovalipollis pseudoalatus (Thiergart) Schuurman 1976Osmundacites wellmani Couper 1953Porcellispora longdonensis (Clarke) Scheuring 1970Pinuspollenites sp.Reticulatisporites muricatus Kosanke 1950Protodiploxipinus fastidiosus (Jansonius) Warrington 1974Staurosaccites quadrifidus Dolby in Dolby and Balme 1976Pseudoillinites platysaccus (Madler) Fisher and Dunay 1984Todisporites marginales Bharadwaj and Singh 1964Retusotriletes hercynicus (Madler) Schuurman 1977Triadispora suspecta Scheuring 1970Staurosaccites quadrifidus Dolby in Dolby and Balme 1976Triadispora sp.Striatoabieites aytugii Visscher 1966Undetermined bisaccatesTodisporites cinctus (Malyavkina) Orlowska-Swolinska 1971Unit BTriadispora crassa Klaus 1964Significant elementsTriadispora falcata Klaus 1964Camerosporites secatus Leschik 1956Triadispora sp.Enzonalasporites vigens Leschik 1956Uvaesporites gadensis Praehauser-Enzenberg 1970‘Lueckisporites’ cf. singhii Balme 1970Verrucosisporites applanatus Madler 1964aPatinasporites densus Leschik 1956Verrucosisporites morulae Klaus 1960Partitisporites novimundanus morphon Van der Eem 1983Undetermined bisaccatesVallasporites ignacii Leschik 1956

Unit CBaltisphaeridium sp.aSignificant elementsMicrhystridium sp.aGliscopollis meyeriana ( Klaus) Venkatachala 1966Accessory elementsGranuloperculatipollis rudis Venkatachala and Goczan 1964Alisporites grauvogelii Klaus 1964Microreticulatisporites fuscus (Nilsson) Morbey 1975Alisporites sp.Partitisporites novimundanus morphon Van der Eem 1983Angustisulcites grandis (Freudenthal ) Visscher 1966Patinasporites densus Scheuring 1970Angustisulcites sp.

Accessory elementsAnapiculatisporites spiniger (Leschik) Reindhardt 1962Anapiculatisporites spiniger (Leschik) Reindhardt 1962Apiculatisporis bulliensis Helby 1973 ex de Jersey 1979Calamospora mesozoica Couper 1958Aratrisporites fimbriatus ( Klaus) Playford and Dettmann 1965Concavisporites crassexinius Nilsson 1958Aratrisporites tenuispinosus Playford 1965Concavisporites toralis (Leschik) Nilsson 1958Baculatisporites comaumensis (Cookson) Klaus 1960Cycadopites follicularis Wilson and Webster 1946Calamospora mesozoica Couper 1958Deltoidospora sp.Cingulizonates rhaeticus (Reindhardt) Schulz 1967Duplexisporites sp.Clavatisporites hammenii (Herbst) de Jersey 1971Marattisporites scabratus Couper 1958Concentricisporites insignis Pautsch 1973Osmundacites wellmanii Couper 1953Converrucosisporites sp.Retitriletes sp.Cuneatisporites radialis Leschik 1956Retusotriletes sp.Cuneatisporites cerinus Dolby and Balme 1976Spheripollenites psilatus Couper 1958Cycadopites follicularis Wilson and Webster 1946Todisporites spp.Cyclogranisporites sp.

Unit DDeltoidospora mesozoicus (Thiergart) Schuurman 1977Significant elementsDeltoidospora minor (Couper) Pocock 1970Araucariacites australis Cookson 1947Duplicisporites granulatus Leschik 1956


Table 1 (continued ) dinocyst assemblage, can be reasonably assignedto the Norian.Chasmatosporites apertus Nilsson 1958

Clavatipollenites hughesii Couper 1958, sensu Schulz 1967Heibergella aculeata Bujak and Fisher 1976a 6.3. AmmonitesHeibergella salebrosacea Bujak and Fisher 1976aMicrhystridium spp.a The fossils have been collected from limestone

Accessory elementsblocks (Unit H ) ranging in size from 0.2 to 1 m3.Cycadopites follicularis Wilson and Webster 1946Though many blocks contain different fossil layers,Deltoidospora sp.

Uvaesporites sp. their faunas have been treated collectively and areVitreisporites pallidus Reissinger (Nilsson 1958) now mixed. Therefore, several samples containUndetermined smooth spore ammonites of different age (resp. zones), confirm-

ing stratigraphic condensation. Detailed bed-by-a Marine elements.bed collections of fossils otherwise have shown anormal, e.g. uncondensed ammonite zonal succes-sion with, for example, a total Norian rock thick-ness of 3 m (Tatzreiter, 1981; Krystyn and

Patinasporites densus and Partitisporites novimun- Wiedmann, 1986). The fossils are generally welldanus morphon, together with the post-Carnian G. preserved and often contain a thin FeMn-oxidemeyeriana and G. rudis, suggests a Norian age, coating. This preservation points to a highly oxi-possibly Lower to Middle Norian, for Unit C. dizing primary environment with a very low sedi-

mentation rate (Halstatt facies).All faunas from Noe Tobe and Noe Bihati listedUnit D

below are of Upper Triassic age and, with theexception of TM80 (which is Upper Carnian), ofThe palynological assemblage from the grey

marls of Unit D is characterized by well-preserved Norian age (Table 2). The overrepresentation ofNorian samples by both number (90%) and faunalmarine elements. The dominant dinocysts are

Heibergella salebrosacea and H. aculeata, and quality is remarkable as the area is historicallyfamous for its almost complete Triassic ammonoidamong the Acritarchs, Micrhystridium spp.

Sporomorphs are represented by Chasmatosporites record (Welter, 1914, 1915, 1922; Diener, 1923;Arthaber, 1927). Blocks of Norian age may there-apertus, Araucariacites australis, Clavatipollenites

hughesii, Cycadopites follicularis, Vitreisporites pal- fore be more common than others according toour record. The historic data, however, are impor-lidus, Uvaesporites sp., Deltoidospora sp., and

undetermined smooth spores. tant as they demonstrate the onset of the Hallstattfacies in the early Triassic and the development ofBatten and Koppelhaus (1996) reported

Chasmatosporites apertus as ranging from the ?Late a stable pelagic plateau sedimentation for at least40 Ma from the Lower Triassic until the base ofNorian to Bathonian, Clavatipollenites hughesii,

from the ?Rhaetian to the Late Oxfordian, and the Jurassic.The full range of ages for the samples (resp.Araucariacites australis as starting from the

?Rhaetian. The relatively abundant dinocysts in blocks) is shown in Table 2, in relation to theNorian Tethyan geological time-scale. Norianthe association yielded additional stratigraphic

information. The species Heibergella salebrosacea ammonites have been described from Timor byWelter (1914) and Diener (1923), with a recentand Heibergella aculeata were so far recorded only

in marine sediments of Norian age from the revision by Tatzreiter (1981). Most of the collectedspecies (Plate IV; Table 2) are therefore wellSverdrup Basin (Arctic Canada) (Bujak and

Fisher, 1976; Helby et al., 1987); West Timor is known from the island, and all have a distinctTethyan or low paleolatitude (LPL) distribution.thus the second known locality for these species.

In spite of the scattered records of H. salebrosacea They are further known from the Himalayas(Mojsisovics, 1899; Diener, 1908; Krystyn, 1982),and H. aculeata, the age of Unit D, based on the


Table 2Ammonites and other fossil assemblages from the blocks of Unit H, in relation to the Upper Triassic time-scale

Locality Sample Ammonites and bryozoan Conodonts Age

Noe Tobe TM18 Stenarcestes subumbilicatus Bronn Upper NorianHeterastridium conglobatum Reuss Sevatian

Noe Bihati TM74 Rhacophyllites neojurensis (Quenst.) Middle NorianHalorites sp. Alaunian 3Arcestes sp.

TM73 Halorites macer Mojs.Amarassites semiplicatus (Hauer)Thetidites huxleyi Mojs.Paracladiscites multilobatus (Bronn)Pinacoceras metternichi (Hauer)Rhacophyllites neojurensis (Quenst.)Paranautilus sundaicus WelterHeterastridium conglobatum Reuss

TM72B Halorites macer Mojs.H. sapphonis Mojs.Amarassites semiplicatus (Hauer)A. parmenidis DienerBrouwerites intermedius (Welter)Steinmannites timorensis WelterArgosirenites dianae Mojs.Cladiscites beyrichi WelterC. neortus (Mojs.)Paracladiscites multilobatus (Bronn)Pinacoceras cf. metternichi (Hauer)Arcestes div. sp.Stenarcestes sp.Rhacophyllites neojurensis (Quenst.)Gonionautilus quenstedti (Hauer)Clydonautilus noricus Mojs.Paranautilus simonyi (Hauer)

TM71B Halorites macer Mojs. Norigondolella steinbergensis (Mosher)Amarassites semiplicatus Hauer Epigondolella slovakensis Kozur and MockAlloclionites cf. aries Mojs.Argosirenites cf. dianae Mojs.Leislingites archibaldi (Mojs.)Helictites geniculatus (Hauer)Episculites subdecrescens (Mojs.)Paracladiscites multilobatus (Bronn)Placites oxyphyllus (Mojs.)Pinacoceras metternichi (Hauer)Arcestes sp.Rhacophyllites neojurensis (Quenst.)Megaphyllites insectus (Hauer)Atractites alveolaris (Quenst.)

TM70 Halorites macer Mojs. Norigondolella steinbergensis (Mosher)Amarassites semiplicatus (Hauer) Epigondolella slovakensis Kozur and MockAlloclionites procerus Tatzreiter

TM72A Didymites subglobus Mojs. Middle NorianTM71A Distichites hollandi Diener Alaunian 1

D. cf. falcatus DienerParadistichites sp.Ectolcites pseudoaries (Hauer)Argosirenites sp.


Table 2 (continued )

Locality Sample Ammonites and bryozoan Conodonts Age

Parathisbites scaphitiformis HauerJellinekites sp.Placites cf. oxyphyllus (Mojs.)Arcestes sp.

Noe Tobe TM17 Malayites cf. paulckei Diener Norigondolella hallstattensis (Mosher) Lower NorianM. singularis Welter Epigondolella triangularis Budurov Lacian 2Waldthausenites sp.Cladiscites angustus GamsjageRhacophyllites sp.Arcestes sp.Asteroconites radiolaris Teller

Noe Bihati TM69 Griesbachites inflatus Welter Epigondolella quadrata Orchard Lower NorianCladiscites crassestriatus (Mojs.) Lacian 1C. angustus Gamsj.Pinacoceras sp.Rhacophyllites zitteli Mojs.Gonionautilus malayicus WelterAsteroconites radiolaris Teller

TM80 Indonesites dieneri Welter Upper Carnian Tuvalian 2

Oman (Tozer and Calon, 1990; Blendinger, 1991, and TM71, they confirm the Middle Norian(ALAUNIAN) age established by the ammonites.1995) and from the Western Tethys (Tatzreiter,

1978; Krystyn 1980).

6.4. Conodonts 7. Sequence stratigraphy

In terms of sequence stratigraphy, the UpperSeveral ammonoid samples of the condensedlimestone (Unit H), or samples from the matrix, Triassic series of the Allochthonous complex of

West Timor shows two major depositionalwere dissolved in formic acid; they delivered richconodont faunas dominated by the platform sequences (DS1 and DS2), according to facies

analysis and biostratigraphic data (Fig. 6).genera Norigondolella and Epigondolella (Plate V ).In the Noe Tobe area, between the Niki Niki The basal part of the Triassic succession ( Units

A and B) shows a regressive trend. Unit A repre-and Soe villages, at the mouth of a small tributaryof the river Bunu (Noe Bunu), one isolated block sents a condensed section (including a maximum

flooding surface) within either a transgressive sys-(TM17) has yielded, together with the ammonites(Table 2) dated from the Lower Norian (LACIAN tems tract (TST) or an early highstand systems

tract (HST ). The overlaying Unit B is interpreted2), a conodont association of the same age withNorigondolella hallstattensis (Mosher) and as the HST of the DS1 depositional sequence. The

age of DS1 is Carnian, based on palynomorphsEpigondolella triangularis Budurov.In the Noe Bihati section (Baun area), three assemblages. The regressive trend of Unit B, as

indicated by the predominance of land plantmatrix samples (TM69, TM70, TM71; Fig. 4) havebeen processed for conodonts; TM69 contains the remains, and a high percentage of sporomorphs

and inertinite, probably reflects a relative sea-levelLower Norian (LACIAN 1) Epigondolella quad-rata Orchard; Norigondolella steinbergensis fall (Lowstand), or the exposure of a distant

shallow platform (e.g. Australian margin, Rohl(Mosher), and Epigondolella slovakensis Kozurand Mock have been recorded from samples TM70 et al., 1991, 1992).


PLATE IV


Unit C, which represents the TST of DS2, was (?) pelagic molluscs, then shallow-water reefal car-ates (Bogal Formation). These limestones suffereddeposited during a relative sea-level rise. Unit D,

particularly the nodular limestone at the top of a major drowning event, as Middle Jurassic deep-sea shales were then deposited (Yefbie Formation).the unit, is interpreted as an early HST. Finally,

the uppermost portion of the series, Unit E, repre- South of Timor, from the Arafura sea to theExmouth Plateau, syntheses of Schluter andsents a late HST. The age of DS2 is Norian; the

top of the depositional sequence is probably upper- Fritsch (1985), Bradshaw et al. (1990),Struckmeyer et al. (1990, 1993), Stephenson andmost Norian to lowermost Rhaetian (presence of

the radiolaria Livarella valida). Cadman (1994) and McConachic et al. (1996)indicate that Middle to Late Triassic deposits areA correlation of the Triassic series with the

cycle chart of Haq et al. (1987) is tentatively mainly siliciclastics, from marginal marine (deltaderived dominating sediments) to continental envi-proposed, based on micropaleontological data. In

terms of global environmental changes, it is pos- ronments (e.g. Upper Triassic Malita Formation).These deposits suffered a major tensional tectonicsible to demonstrate that the major sea-level varia-

tions are also recorded in the Triassic basinal event during Early Jurassic times, and the Jurassicdeposits are often unconformably overlying thesediments of West Timor (Fig. 6).oldest rocks.

Comparing the sedimentary evolution of theinvestigated area in West Timor, similarities with8. Comparisons with the Australian marginthe Australian margin do not clearly appear, asfacies still remain of a deep-sea origin, with aSince the island of Timor is classically consid-

ered to be an external part of the Australian Ladinian to Norian tensional tectonic event,which, out of Timor, is poorly documented.margin, it is reasonable to compare the Triassic of

Timor with that of the many regions of the inten- In the NW coast of Australia, for Audley-Charles (1983) and Sawyer et al. (1993), thesively studied Australian margin.

In Papua New Guinea, most of the Australian formation of the Mount Goodwin (BonaparteBasin, SE of Timor) would be the equivalent ofshelf was emerged during Middle–Late Triassic

times; in the Pacific margin, siliciclastic fluvio- the Lower Triassic silts, black shales, clays andmarly clays of Timor, and the High Londonderrydeltaic to shallow marine sediments were depos-

ited, including local reefal carbonate platform formation the equivalent of the Ladinian toCarnian clays and limestones of Timor. The terrig-deposits in Misool island (W of Irian Jaya) and

in the Kubor block (Papuasia) (Pigram et al., enous deposits of the Malita Graben (Rhaetian toLiassic) are much more arenaceous than their1982; Struckmeyer et al., 1993). In Misool island,

the lithostratigraphic succession includes turbiditic supposed equivalents in Timor.More convincing is the palaeogeographicfine-grained siliciclastics with Carnian to Ladinian

PLATE IV

1. Stenarcestes subumbilicatus Bronn. Sample TM18, Noe Tobe; max. diam. 5 cm. Upper Norian (Sevatian).2. Didymites subglobus Mojsisovics. Sample TM72A, Noe Bihati; max. diam. 5,3 cm. Middle Norian (Alaunian 1).3. Parathisbites scaphitiformis Hauer. Sample TM71A, Noe Bihati; max. diam. 3,2 cm. Middle Norian (Alaunian 1).4. Distichites hollandi Diener. Sample TM71A, Noe Bihati; max. diam. 6,7 cm. Middle Norian (Alaunian 1).5. Amarassites semiplicatus (Hauer). Sample TM72B, Noe Bihati; max. diam. 8,5 cm. Middle Norian (Alaunian 3).6. Argosirenites cf. A. dianae Mojsisovics. Sample TM71B, Noe Bihati; max. diam. 6,7 cm. Middle Norian (Alaunian 3).7. Brouwerites intermedius ( Welter). Sample TM72B, Noe Bihati; max. diam. 8,3 cm. Middle Norian (Alaunian 3).8. Amarassites parmenidis Diener. Sample TM72B, Noe Bihati; max. diam. 7,2 cm. Middle Norian (Alaunian 3).9. Halorites macer Mojsisovics. Sample TM72B, Noe Bihati; max. diam. 9,6 cm. Middle Norian (Alaunian 3).10. Steinmannites timorensis Welter. Sample Tm72B, Noe Bihati; max. diam. 11,2 cm. Middle Norian (Alaunian 3).


PLATE V


intertation of Mac Kenzie (1987), which does not platform areas in Australia and Indonesia remaindifficult to correlate with that of Timor.show any notable similitude of Timor with the

Australian margin: in Australia, the Middle Conclusively, in the current state of knowledge,the initial adherence of the Triassic series of theTriassic appears to be a period of regression, not

observed in Timor, and the Upper Triassic shows Allochthonous of Timor to the Australian marginis highly questionable. The studied area in Timorshallow-water deposits, while the characteristic

radiolarites of Timor are indicative of the deepen- underwent an original sedimentary evolution,rather different from that of the Australian margin,ing of this portion of passive margin. These data

are also supported by the results of Bradshaw and of the microcontinents of the Banda Sea.More precise geodynamic reconstructions foret al. (1988) and Kraus and Parker (1979).

On the same continental margin, the Wombat Triassic times are now necessary for an accurateinterpretation of the pelagic Triassic deposits ofPlateau exhibits a different Middle–Late Triassic

succession that was studied during the ODP marine Timor, regarding carbonate platform areas andsiliciclastic deposits of the Australian margin. Asurvey Leg. 122 (sites 761, 764, 759, 760). There,

numerous studies (e.g. Dumont and Rohl, 1991; similar problem is the origin of the Triassic turbidi-tic series of the Buton Island in the western partRohl et al., 1991; Borella et al., 1992; Dumont,

1992) indicate a Carnian–Norian siliciclastic suc- of the Banda Sea (Smith and Silver, 1991).cession (delta dominated sequence), then aRhaetian shallow-water reefal carbonate succes-sion. The Triassic rocks were then uplifted anderoded, prior to a major drowning event duringthe Jurassic. These carbonate rocks are shown to Acknowledgementsbe rather similar to those of some of the microcon-tinents of the Banda Sea (Sulawesi, Sinta Ridge, This work was financially supported by the

Swiss National Science Foundation (L.Z. GrantsBuru, Seram), as discussed in Martini et al. (1997).Even if it is possible to identify major regressions N° 20-41881.94 and 20-50577.97), and the French

PICS–Indonesia Project. G. Roselle (University ofat around −224, −215 and −211 Ma in Timor(this work), in Sulawesi (Martini et al., 1997) and Bern), Profs M. Gaetani and M. Sarti are thanked

for their helpful reviews and J. Metzger for theon the Wombat Plateau (Dumont, 1992), thegeneral sedimentary evolution of the carbonate graphical assistance.

PLATE V

1–2. Norigondolella hallstattensis (Mosher). Sample TM17, Noe Tobe. Lateral and upper view, 880 mm. LowerNorian (Lacian 2).

3–4, 5–6. Epigondolella triangularis Budurov. Sample TM17, Noe Tobe. Lateral and upper views.3–4. 710 mm.5–6. 730 mm. Lower Norian (Lacian 2).7–8, 9–10. Epigondolella quadrata Orchard. Sample TM69, Noe Bihati. Lateral and upper views.7–8. 800 mm.9–10. 580 mm. Lower Norian (Lacian 1).11–12, 15–16, 19–20. Norigondolella steinbergensis (Mosher). Sample TM70+71, Noe Bihati. Lateral and upper views.11–12. 810 mm.13–14. 720 mm.15–16. 1050 mm. Lower Norian (Lacian 3).13–14, 17–18, 21–22. Epigondolella slovakensis Kozur and Mock. Sample TM70+71, Noe Bihati. Lateral and upper views.17–18. 610 mm.19–20. 540 mm.21–22. 670 mm. Lower Norian (Lacian 3).


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