Marine and Petroleum Geology: D.P. Gold, L.T. White, I. Gunawan, M.K. Boudagher-Fadel

Marine and Petroleum Geology 86 (2017) 1133e1158
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Marine and Petroleum Geology

journal homepage: www.elsevier.com/locate/marpetgeo
Research paper
Relative sea-level change in western New Guinea recorded by regional

biostratigraphic data
D.P. Gold a, *, L.T. White a, b, I. Gunawan a, c, M.K. BouDagher-Fadel d
a
Southeast Asia Research Group, Department of Earth Sciences, Royal Holloway University of London, Egham, Surrey, TW20 0EX, UK
b
School of Earth and Environmental Sciences, University of Wollongong, Wollongong, NSW, 2522, Australia
c
Institut Teknologi Bandung, Jl. Ganesha No.10, Lb. Siliwangi, Coblong, Kota Bandung, Jawa Barat, 40132, Indonesia
d
Department of Earth Sciences, University College London, Gower Street, London, WC1E 6BT, UK
a r t i c l e i n f o a b s t r a c t
Article history: We present new biostratigraphic analyses of approximately 200 outcrop samples and review biostrati-
Received 8 June 2017 graphic data from 136 public domain exploration wells across western New Guinea. Biostratigraphic ages
Accepted 17 July 2017 and palaeodepositional environments were interpreted from occurrences of planktonic and larger
Available online 19 July 2017
benthic foraminifera, together with other fossils and environmental indicators where possible. These
data were compared with existing geological maps and exploration well data to reconstruct the palae-
Keywords:
ogeography of western New Guinea from the Carboniferous to present day. In addition, we used the
Tectonics
known bathyal preferences of fossils to generate a regional sea-level curve and compared this with global
Foraminifera
Palaeogeography
records of sea-level change over the same period. Our analyses of the biostratigraphic data identified two
Biogeography major transgressive-regressive cycles in regional relative sea-level, with the highest sea levels recorded
Eustasy during the Late Cretaceous and Late Miocene and terrestrial deposition prevalent across much of western
New Guinea during the Late Paleozoic and Early Mesozoic. An increase in the abundance of carinate
planktonic foraminifera indicates a subsequent phase of relative sea-level rise during a regional trans-
gressive event between the Late Jurassic and Late Cretaceous. However, sea-levels dropped once more
during a regressive event between the Late Cretaceous and the Paleogene. This resulted in widespread
shallow water carbonate platform development in the Middle to Late Eocene. A minor transgressive
event occurred during the Oligocene, but this ceased in the Early Miocene, likely due to the collision of
the Australian continent with intra-Pacific island arcs. This Miocene collision event resulted in wide-
spread uplift that is marked by a regional unconformity. Carbonate deposition continued in platforms
that developed in shallow marine settings until these were drowned during another transgressive event
in the Middle Miocene. This transgression reached its peak in the Late Miocene and was followed by a
further regression culminating in the present day topographic expression of western New Guinea.
© 2017 Elsevier Ltd. All rights reserved.
1. Introduction numerous tectono-thermal events during the Paleozoic, Mesozoic

and Cenozoic (e.g. Visser and Hermes, 1962; Pieters et al., 1983;
New Guinea has represented the northernmost boundary of the Davies and Jaques, 1984; Pigram and Davies, 1987; Pigram and
Australian Plate from the present until at least the Permian Symonds, 1991; Baldwin and Ireland, 1995; Baldwin et al., 2004,
(perhaps as early as the Carboniferous). During this time New 2012; Davies, 2012; Bailly et al., 2009; Holm and Richards, 2013;
Guinea was part of an Andean-style continental arc system that Holm et al., 2015, 2016; François et al., 2016). However, much of
extended around a large portion of Gondwana (Charlton, 2001; the geology of New Guinea is also dominated by siliciclastic and
Hall, 2002, 2012; Hill and Hall, 2003; Crowhurst et al., 2004; carbonate deposition during seemingly long periods of quiescence
Metcalfe, 1998, 2009; Gunawan et al., 2012, 2014; Webb and (Pieters et al., 1983; Pigram; Visser and Hermes, 1962; Fraser et al.,
White, 2016). This long-lived plate boundary records evidence of 1993; Hill, 1991; Davies, 2012; Baldwin et al., 2012). We focus on the
age and depositional environment of these sediments in western
New Guinea, an area that is relatively underexplored, with the last
* Corresponding author. major geological mapping campaign being conducted in the 1980's
E-mail address: david.patrick.gold@gmail.com (D.P. Gold).
http://dx.doi.org/10.1016/j.marpetgeo.2017.07.016
0264-8172/© 2017 Elsevier Ltd. All rights reserved.
1134 D.P. Gold et al. / Marine and Petroleum Geology 86 (2017) 1133e1158
(e.g. Masria et al., 1981; Pieters et al., 1983; Dow et al., 1986; Pieters et al., 1983; Milsom, 1992). Thus the stratigraphy of the
Atmawinata et al., 1989; Pieters et al., 1989; Dow et al., 1990; Bird's Head can be broadly described as intra-Pacific island arc
Harahap et al., 1990; Pieters et al., 1990; Robinson et al., 1990; material to the north and east, which accreted to Australian con-
Panggabean et al., 1995). We present new biostratigraphic age tinental material to the south and west. The post-collisional stra-
data based on benthic and planktonic foraminifera, as well as facies tigraphy of both domains is reasonably contiguous.
analyses from nearly 200 outcrop samples from western New
Guinea. Where possible, we compared these results with publicly 2. Depositional history of western New Guinea sediments
available hydrocarbon exploration well locations, biostratigraphic
analyses and interpreted depositional environments (e.g. Visser 2.1. Australian plate stratigraphy
and Hermes, 1962; Fraser et al., 1993). The aim of this work was
to better establish the duration and facies distribution of strata to A simplified map showing the distribution of sedimentary,
better understand the spatio-temporal distribution of periods of igneous and metamorphic rocks mapped by Masria et al. (1981);
queisence at the northern margin of the Australian Plate between Pieters et al. (1983); Dow et al. (1986); Atmawinata et al. (1989);
the Carboniferous and present day. We begin by reviewing the Pieters et al. (1989); Dow et al. (1990); Harahap et al. (1990);
existing literature on the geology of western New Guinea. We then Pieters et al. (1990); Robinson et al. (1990); Panggabean et al.
discuss the newly obtained biostratigraphic data as well as data (1995) is shown in Fig. 2. The oldest strata within the Bird's Head
obtained from a meta-study of publically available biostratigraphic consist of variably metamorphosed siliciclastic rocks that were
data from exploration wells, and what these mean for our under- most likely derived from rocks to the south (i.e. eroded Australian/
standing of changing palaeo-environments. Gondwanan crust) (e.g. Decker et al., 2017) (Figs. 2 and 3). The
variably metamorphosed rocks in the Bird's Head Peninsula have
1.1. Geological mapping of western New Guinea poor age control, but were assigned a Silurian-Devonian age from
several graptolites and because these rocks are cross-cut by
The first comprehensive geological mapping of Indonesian New Carboniferous and Permian intrusions (Visser and Hermes, 1962;
Guinea was conducted between 1935 and 1960 by geologists of the Pieters et al., 1983) (Figs. 2 and 3). These sequences are known as
Nederlandsche Nieuw Guinee Petroleum Maatschappij. The results the Kemum and Aisasjur Formations (Fig. 3) and are considered to
of this work are compiled and summarised in Visser and Hermes represent distal and proximal turbidite deposits, respectively
(1962). The observations reported in this work lay the foundation (Visser and Hermes, 1962; Pieters et al., 1983). The low meta-
for the stratigraphy of western New Guinea and remain highly morphic grade turbidite sequences of the pre-Middle Triassic Ligu
relevant, despite this work being completed before the advent of Formation in Misool are potentially equivalent to those classified as
plate tectonics. The stratigraphy and tectonic development of the Kemum Formation (Hasibuan, 2012). Other Devonian to Late
western New Guinea was refined by Indonesian and Australian Proterozoic siliciclastic and carbonate sequences are exposed in
government geologists between 1978 and 1982; the results of parts of Papua New Guinea (e.g. Modio Formation, Tuaba Forma-
which are summarised in Pieters et al. (1983). Subsequent work has tion, Karieum Formation) along with the Late ProterozoiceCam-
predominantly been driven by hydrocarbon or mineral exploration brian metamorphosed basaltic rocks of the Awitagoh and Nerewip
in the region (e.g. White et al., 2014) and broadly consists of reviews formations (Davies, 2012 and references therein) (Fig. 3). The oldest
of the stratigraphy (e.g. Fraser et al., 1993), the regional tectonic carbonate unit in western New Guinea is the Modio Dolomite of the
evolution (e.g. Decker et al., 2009; Baldwin et al., 2012; Davies, Central Ranges. This was deposited during the Devonian or possibly
2012) or targeted geological studies that have broadly focused on as early as the Silurian (Fig. 3; Pieters et al., 1983; Nicoll and Bladon,
the evolution and uplift of basement rocks (e.g. Bailly et al., 2009; 1991; Oliver et al., 1995; Parris, 1994; Cloos et al., 2005; Davies,
François et al., 2016; Webb and White, 2016). 2012).
During the Carboniferous, a phase of magmatism was suggested
1.2. The Bird's Head, Neck, Body and Tail from K-Ar dating of porphyritic dacite and altered porphyritic
igneous rocks from the Melaiurna Granite (Bladon, 1988). Despite
New Guinea is often described to reflect the shape of a bird, this volcanism, the Carboniferous to Permian was a period of
comprising the Bird's Head, Neck, Body, and Tail from west to east, relatively stable paralic sediment deposition, with occasional
respectively (Fig. 1). The Bird's Head and Neck, and part of the Body shallow marine incursions marked by thin limestone beds in New
are within the Indonesian provinces of West Papua and Papua Guinea's Central Range. The Permo-Carboniferous Aifam Group
(formerly known as Irian Jaya). The rest of the Bird's Body and the (Fig. 3) contains various terrestrial and marine deposits (Visser and
Tail are found in Papua New Guinea. The island's peculiar Hermes, 1962; Chevallier and Bordenave, 1986; Dow et al., 1986).
morphology largely reflects the geology and tectonic evolution of This group consists of the Aimau, Ainim and Aiduna formations
the island. For example, the Bird's Neck is largely composed of which collectively consist of conglomerates, red beds and coal
limestones and siliciclastic rocks shortened during the develop- seams that were likely deposited in a terrestrially influenced,
ment of the Lengguru Fold and Thrust Belt (e.g. Bailly et al., 2009; possibly deltaic and/or lacustrine setting (Norvick, 2003). The Aifat
François et al., 2016)(Fig. 1). These deformed rocks form part of a Mudstone, which also forms part of the Aifam Group however most
mountain belt that extends from western New Guinea (the Bird's likely represents deposition in deeper water, perhaps in a basinal
Head), along the Lengguru Fold and Thrust Belt (the Bird's Neck), setting (Pieters et al., 1983).
continuing along the Central Range (the Bird's Body) to the eastern Volcanic activity recommenced or became much more extensive
tip of the island (Bird's Tail) (Fig. 1). Rocks to the south of New during the Triassic. The evidence for this is taken from various
Guinea are primarily of Australian continental affinity whereas granitoids found in the Bird's Head Peninsula and on the western
those to the north consist of ophiolite and island arc volcanics of and southwestern sections of Cenderawasih Bay (Fig. 2). The
Pacific Plate provenance. The two domains are separated by a granitoids include the Netoni Intrusive Complex, Anggi Granite,
central, complex region of juxtaposed fault slices of sediments Wariki Granodiorite, Warjori Granite and this magmatic belt likely
together with variably metamorphosed and granitic rocks. This continues further to the east, along the length of New Guinea (e.g.
juxtaposition marks a suture that formed during arc-continent Bladon, 1988; Crowhurst et al., 2004; Webb and White, 2016).
collision between the Oligocene and Early Miocene (Fig. 1), (e.g. Additional supporting evidence for this Triassic magmatism comes
D.P. Gold et al. / Marine and Petroleum Geology 86 (2017) 1133e1158 1135
Fig. 1. Map of (a) New Guinea and (b) western New Guinea which represents the focus of this study. These indicate the location of various geographic and geological names that are
discussed in the text. A dashed line is also shown in (a). This broadly represents the boundary between basement rocks with an Australian affinity (to the south) and Pacific affinity
(to the north).
Fig. 2. A simplified lithological map of western New Guinea based on the distribution of lithologies shown on earlier GRDC maps and work conducted as part of this study. The map
shows the location of recent sediments; fault and mud volcano melange; siliciclastics; carbonates; volcanics; intrusives; ultramafic and metamorphic rocks. Readers should note
that the map does not provide any indication of the age of the rocks. The map was modified from Masria et al. (1981); Pieters et al. (1989); Robinson et al. (1990); Pieters et al.
(1990); Brash et al. (1991).
from detrital zircon age dates together with volcanic quartz found Cretaceous to Middle Miocene limestones. The NGLG is between
in ash fall and fluvial sequences of the Tipuma Formation 1 km and 1.6 km thick, and crops out in the western Bird's Head, the
(Gunawan et al., 2012, 2014) (Fig. 3). It was likely that the Triassic Lengguru Fold and Thrust Belt, the Central Range and in parts of
magmatism was coeval with carbonate deposition e the closest Papua New Guinea (Brash et al., 1991, Fig. 3). The Waripi Formation
evidence for this is taken from the Late Triassic Manusela and represents the oldest Paleogene strata of the NGLG. These were
Asinepe Limestone formations of Misool and Seram respectively deposited in shallow-water areas of a new Cenozoic basin from the
(Pieters et al., 1983; Martini et al., 2004). The deposition of these middle to late Paleocene (Brash et al., 1991, Fig. 4). However,
sequences continued into the early to middle Jurassic with depo- turbidite deposits of the Daram Formation were deposited in deep-
sition occurring in shallow seas with little siliciclastic input. There water areas to the north of this basin (Norvick, 2003). The Imskin
was a greater and increasing proportion of siliciclastic material Limestone (part of the NGLG) may interfinger with the Waripi
being deposited in the Bird's Head Peninsula during the Jurassic Formation in these deep-water areas (Brash et al., 1991) (Fig. 4). The
and into the Late Cretaceous. This consisted of the deposition of the Cenozoic basin was relatively stable throughout the Eocene,
Tamrau Formation and Kembelangan Group (Fig. 4) which are depositing the shallow-water Faumai and Lengguru Limestones,
broadly equivalent to the shelfal deposits of the Demu and Lelintu while the Imskin Limestone continued accumulating pelagic car-
Formations of Misool (Hasibuan, 1990) (Fig. 4). bonate up until collision with an intra-Pacific island arc between
The Cretaceous siliciclastic units of the Kembelangan Group the Oligocene and Early Miocene (Fig. 4).
include the Jass Formation, Piniya Mudstone and the Woniwogi and
Ekmai Sandstones (Fig. 4). Carbonate deposits in the Bird's Head are 2.2. Pacific Plate and contiguous stratigraphy
not known until the Late Cretaceous (Pieters et al., 1983). These
include Coniacian to Maastrichtian age siliciclastics of the Ekmai Within the intra-Pacific island arc, carbonate deposition was
Sandstone which pass laterally into the deep-water pelagic car- restricted to patch reefs developed around eroded volcanoes
bonates of the Simora Formation (Fig. 4; Brash et al., 1991). Frag- known from the Eocene age Auwewa Formation (Fig. 4). This per-
ments of inoceramid bivalves within the base of the conformably sisted until the OligoceneeEarly Miocene collision between an is-
overlying Waripi Formation suggest a Late Cretaceous age for the land arc and New Guinea (Wilson, 2002). Following collision,
base of this unit. carbonate platform development was widespread across much of
From the Late Cretaceous to early Paleogene there is a distinct the Bird's Head Peninsula. Early to middle Miocene platform car-
change from siliciclastic to carbonate deposition recorded across bonates of the Kais and Maruni Limestones as well as the Wainu-
the Bird's Head (Fig. 4). Visser and Hermes (1962) proposed the kendi and Wafordori Formations (Figs. 2 and 4), were subsequently
name ‘New Guinea Limestone Group’ (NGLG) to include Late drowned during a middle to late Miocene transgressive event that
abruptly terminated platform accumulation (Brash et al., 1991;

Gold et al., 2014; Baillard et al., 2017). During the Pliocene, or
very latest Miocene, rapid uplift attributed to major thrusting,
folding (Wilson, 2002) and strike-slip faulting prevailed in the
Bird's Head Peninsula, with the strike-slip faulting resulting in the
formation of several sedimentary basins (Pieters et al., 1983). Areas
that were uplifited due to collision eroded rapidly, filling these
basins with siliciclastic sediment. Only the islands of Misool and
Biak remained starved of siliciclastic sedimentation permitting
deposition of platform carbonates of the Wardo, Korem and
Mokmer Formations (Fig. 4) in relatively clear waters (Pieters et al.,
1983; Wilson, 2002).
3. Methodology
This paper presents the results of several field campaigns con-

ducted by the Southeast Asia Research Group (SEARG), Royal Hol-
loway University of London, in the Bird's Head Peninsula of
Indonesian New Guinea between 2010 and 2016. Over these cam-
paigns nearly 200 samples were collected from the New Guinea
Limestone Group and other sedimentary units. These include a
mixture of spot samples as well as samples from logged strati-
graphic sections (Supp. Data 1). All samples were thin sectioned
and examined for petrography and biostratigraphic dating using
planktonic and larger benthic foraminifera. Of these, 198 samples
yielded well-constrained biostratigraphic ages (Supp. Data 1). Ages
are assigned using planktonic foraminiferal zones of Blow (1979),
Berggren and Miller (1988) and Berggren et al. (1995), recali-
brated to Wade et al., (2011) sub-tropical planktonic foraminiferal
zones. Larger benthic foraminiferal zones are assigned to the Indo-
Pacific ‘letter stages’ of Adams (1965, 1970), later refined by
BouDagher-Fadel (2008) and Lunt (2013). We subdivided the
biostratigraphic results into 19 time intervals to show the palae-
ogeographic evolution of western New Guinea between the
Carboniferous and Pleistocene.
Palaeogeographic reconstructions were determined using the
bathymetric preferences of organisms (Hallock and Glenn, 1986;
Van Gorsel, 1988; Beavington-Penney and Racey, 2004; Murray,
2006; BouDagher-Fadel, 2008, 2015; Lunt, 2013) observed in each
sample. The palaeogeographic maps presented here have been
subdivided into five relative bathymetries according to the bathy-
metric preferences assigned to samples with depth-diagnostic
foraminiferal assemblages (Fig. 5). Where heterogeneous deposi-
tional environments were interpreted at a single locality, the modal
depositional setting for that time and location is recorded in the
gross depositional maps.
In addition to the biostratigraphic ages and palaeoenvironments
determined from our field studies, we also reinterpreted
biostratigraphic and wireline log data, stratigraphic columns and
existing palaeogeographic interpretations. This includes reinter-
preting the regional stratigraphy of individual reef complexes
within the Salawati and Bintuni basins as well as 136 public domain
hydrocarbon exploration wells (Fig. 6 and Supp. Data 1). Strati-
graphic intervals within the wells were assigned to the relative
bathymetry scheme using records of foraminiferal occurrences that
meet the criteria laid out in Fig. 5.
All of these data were used to produce a series of palaeogeo-
graphic maps. The depositional bathymetries of samples and well
intervals interpreted for each time slice were plotted using ArcGIS
so that the spatial distribution of facies could be compared with
existing palaeogeographic maps of the region (Visser and Hermes,
1962; Audley-Charles, 1965, 1966; Vincelette, 1973; Redmond and
Fig. 3. Simplified stratigraphy of the Silurian to Jurassic rocks of western New Guinea,
from Misool in the west (left hand side), through mainland West Papua (broadly from
Koesoemadinata, 1976; Collins and Qureshi, 1977; Gibson-Robinson
west to east) and Yapen island. and Soedirdja, 1986; Brash et al., 1991; Norvick, 2003; Golonka
et al., 2006, 2009). The new palaeogeographic maps were overlain
Fig. 4. Simplified stratigraphy of the Cretaceous to Recent rocks of western New Guinea, from Misool in the west (left hand side), through mainland West Papua (broadly from west
to east) to the islands of Biak, Supiori and Yapen.
Fig. 5. The bathymetric boundaries used in the palaeogeographic reconstructions are derived from environmental preferences of foraminifera observed in this study. Thick lines
indicate environments in which foraminifera are abundant, thin lines indicate environments in which they also occur infrequently. Environmental preferences are based on field
data and Be (1977), Hallock and Glenn (1986), Van Gorsel (1988), Brash et al., 1991; BouDagher-Fadel (2008, 2015), Beavington-Penney and Racey (2004), Lunt (2013).
on the present day configuration of western New Guinea (e.g. Consequently, we do not attempt the palinspastic restoration of
Visser and Hermes, 1962; Audley-Charles, 1965, 1966; Gibson- structural features, such as the displacement of faults or large-scale
Robinson and Soedirdja, 1986; Brash et al., 1991) as most of New rotation of crustal fragments, nor the restoration of plate fragments
Guinea has been a part of the Australian plate for a considerable (e.g. Norvick, 2003; Golonka et al., 2006, 2009; Charlton, 2010; Hall,
time, with minimal relative movement since at least the Permian 2012). While the maps we developed are somewhat simplified in
(Audley-Charles, 1965, 1966; Gunawan et al., 2012, 2014). terms of the region's tectonic history, our aim was to produce a
Fig. 6. Location of hydrocarbon exploration wells were data were reinterpreted as part of this study. The numbers refer to the name of a particular well. Further details about each
well and the references with information on these public domain wells are provided in Supp. Data 1.
series of maps that could be used to identify the present day dis- Phanerozoic. This was produced by calculating the maximum,
tribution of potential hydrocarbon plays and as an independent minimum and average bathymetry of all biostratigraphic control
means to assess periodicity of localised tectonic driven uplift/sub- points (i.e. outcrop samples and well locations) analysed within a
sidence events compared to global changes in sea level. specific period of time. The “error bars” we report simply show the
In addition to the paleogeographic maps, we also developed a range of bathymetries within the time period. This regional relative
regional relative sea-level curve for Western New Guinea for the sea-level curve was then compared to global sea-level curves (e.g.
Haq and Al-Qahtani, 2005; Müller et al., 2008; Snedden and Liu, and are interpreted here to represent shallow water deposits
2010) to assess potential timing of tectonic events. (<20 m water depth). Triassic marine rocks are also reported from
Misool (Pieters et al., 1983), including the presence of Norian age
4. Results and discussion of palaeogeographic reefs (Fig. 7c; Van Bemmelen, 1949; Visser and Hermes, 1962;
reconstructions Audley-Charles, 1966). In addition, we also consider that an
Andean-style magmatic arc extended along the length of New
The following sections present the results of the palaeogeo- Guinea throughout the Triassic. This is based on igneous zircons
graphic reconstructions and discuss how these maps compare to within the fluvial sequences of the Tipuma Formation, as well as a
previously published work from similar studies. The data used to belt of Triassic-aged granitoids that span the length of New Guinea
generate palaeogeographic reconstructions are listed in Supp. Data and are interpreted to represent the uplifted magma chambers of
1. the volcanic arc (e.g. Crowhurst et al., 2004; Gunawan et al., 2012;
Webb and White, 2016).
4.1. Carboniferous
4.4. Early Jurassic
Conglomerates, red beds and coal seams occur in many of the 14
study wells that intersect the formations of the Aifam Group The deposition of the Tipuma Formation continued until the
(Fig. 3). This suggests the presence of widespread terrestrial Early Jurassic (Visser and Hermes, 1962; Pieters et al., 1983;
depositional settings across the Bird's Head and Neck during the Gunawan et al., 2012). Consequently, a narrow zone of terrestrial
Carboniferous (Fig. 7; Pieters et al., 1983; Fraser et al., 1993; Norvick, deposits is interpreted to extend from the Bird's Head, into the
2003). Carboniferous corals observed from the Aifam Group in the Bird's Neck and Bird's Body (Fig. 7d), and possibly farther into
central Bird's Head (Kato et al., 1999) and from outcrops of the Australia and eastward along the Sula Spur. By the Early Jurassic
Aiduna Formation (Martodjojo et al., 1975; Oliver et al., 1995) open marine strata were being deposited on what is now the island
suggest the presence of shallow water, photic, settings surrounding of Misool (Visser and Hermes, 1962). Deep water clays and marls
the terrestrial zone. are also reported along the northern margin of a landmass
The terrestrial zone is likely to have been associated with a extending from the Bird's Head and Neck, and centre of the Body
magmatic arc considering the porphyritic volcanic rocks of the (Audley-Charles, 1966; Norvick, 2003). Therefore, water depths
Melaiurna Granite dated by Bladon (1988) (Fig. 7a). If a magmatic between 50 m and 100 m are interpreted to surround the central
arc was active at this time then it is likely that deeper water con- New Guinea landmass (Fig. 7d).
ditions could be found further to the north (Fig. 7). This subduction
zone would have likely consisted of a ~southward-dipping (relative 4.5. Middle Jurassic
to the long-axis of the island), dehydrating, Proto-Pacific slab.
The terrestrial deposition recorded over a ~28 Ma period during
4.2. Permian the Late Triassic to Early Jurassic was succeeded by deeper water
sedimentation during a transgressive event in the Middle Jurassic
Permian deposits of western New Guinea are distributed within (Audley-Charles, 1966; Pieters et al., 1990; Lunt and Djaafar, 1991;
a narrow terrestrial zone, extending across the central Bird's Head Gunawan et al., 2012, Fig. 7e). This transgression likely led to the
in the north and south- and westward into the Bird's Neck and Body submergence of the Sula Spur. This increase in relative sea-level
(Fig. 7b). This terrestrial zone contains the land plants Glossopteris also reduced the land area of what is now western New Guinea,
and Gangamopteris plants, reported to stretch from the West Papua leading to the separation of the Bird's Head and Neck (Fig. 7e), as
to Papua New Guinea (Fontaine, 2001). Ten wells contain terrestrial was proposed by Norvick (2003). These newly formed islands were
deposits comprising combinations of red beds, coals, plants and separated by a narrow 50 m-100 m deep seaway that accumulated
freshwater palynomorphs. shelfal clastic deposits (Fig. 7e). Deeper water settings are inter-
The Permian landmass of New Guinea was surrounded by preted to have existed along the northern New Guinea margin, as
shallow water units, interpreted to have been deposited in water supported by neritic clays found along today's northern coast e as
depths no greater than 20 m (Fig. 7b). Data from 13 wells record was reported and proposed by Norvick (2003).
occurrences of delta front material and shallow water limestones Terrestrial deposits are interpreted from six wells in the central
with fusuline-algal assemblages similar to that of Ratburi Lime- Bird's Head and southern Bird's Neck, based on the presence of
stone in peninsular Thailand (Dawson, 1993; Fontaine, 2001). continentally derived palynomorphs. A deltaic system to the west
Deeper water settings are interpreted to the north of the landmass of the northern landmass (Fig. 7e) is recorded from the presence of
where low-energy, fine-grained siliciclastics and carbonates of the fluvio-deltaic sediments within the CS-1X well as well as delta
Ainim Formation and Aifat Mudstone outcrop. plain coals and organic claystones within the Inanwantan sequence
(Fraser et al., 1993). These two islands were flanked by shallow seas
4.3. Triassic with water depths no greater than 20 m, according to sequences
observed in 18 wells. Water depths in excess of 50 m are delineated
The only sedimentary unit in western New Guinea that is by outcrops of the Kopai Formation.
Triassic in age is the Tipuma Formation (Gunawan et al., 2012). The Kopai Formation consists of deep-water black shales and
These rocks were deposited within an arid continental setting limestones (Pieters et al., 1983). Black shales from the Kopai For-
comprising unfossiliferous red-bed sequences (Visser and Hermes, mation contain a common ‘Macrocephalites’ ammonite assemblage
1962; Pieters et al., 1983) and fluvial deposits (Gunawan et al., 2012, close the village of Wendesi. This assemblage includes typical North
2014). This is supported by the presence of oxidised sediments and Gondwanan species including Macrocephalites keeuwensis, Sphaer-
continentally derived palynomorphs reported within many of the oceras boehmi and Holcophylloceras indicum (Fig. 8). This ‘Macro-
hydrocarbon exploration wells (Fig. 7c). Together, the field- and cephalites’ ammonite assemblage is assigned a Bathonian-Callovian
well data indicate that terrestrial deposition was widespread across age (Westermann and Callomon, 1988; Westermann, 1992, 2000;
much of western New Guinea (and Seram) during the Triassic Van Gorsel, 2012). These sequences were deposited within a
(Fig. 7c). Other wells contain paralic and/or supralittoral sediments distal, deep, open marine setting (Van Gorsel, 2012). This
Fig. 7. Palaeogeographic reconstructions of western New Guinea, showing the paleogeographic evolution in the (a) Carboniferous; (b) Permian; (c) Triassic; (d) Early Jurassic; (e)
Middle Jurassic, and the (f) Late Jurassic. These maps are based on the synthesis of biostratigraphic data and interpreted paleodepositional environments from public domain well
data, biostratigraphic reports, regional geology, sedimentological interpretations and new outcrop data. The number of data points used for each map are indicated in each time slice
(e.g. n ¼ ‘x’) and are shown as white dots. These data provide readers with some indication of our level of certainty for each reconstructions/region.
west of the northern landmass is interpreted to persist into the Late

Jurassic due to the presence of sediments reported within the CS-
1X well (Fig. 7f). Deep-water settings continued to encroach
around the margins of the two western New Guinea islands
throughout the Jurassic due to the continued rise in sea-level. These
settings are delineated by outcrops of the Woniwogi, Kopai, Tam-
rau, Demu and Lelinta formations, interpreted as deep-water ma-
rine deposits (Pieters et al., 1983; Hasibuan, 1990). Wells that
intersect Late Jurassic strata comprise glauconitic and argillaceous,
fine-grained, distal sediments and bathyal agglutinated forami-
nifera such as Glomospira spp, and Trochammina spp.
4.7. Early Cretaceous
By the Early Cretaceous, formerly subaerially exposed regions of

western New Guinea were totally submerged beneath water depths
in excess of 100 m (Fig. 9a). This is supported by the presence of
widespread deep marine deposits of the Piniya Mudstone and
Woniwogi Formation across the central Bird's Head (Pieters et al.,
1983). Widespread deep water sedimentation is also supported
by ammonites and belemnites within the Kembelangan-1 well
(Visser and Hermes, 1962) and carinate Globotruncanid planktonic
foraminifera, such as Praeglobotruncana spp., Paraglobotruncana
spp. and Rotalipora spp., in the Kembelangan-1 well. A bathymetric
gradient shallows towards the south-west with interpreted water
depths between 50 m and 100 m (Fig. 9a). This is based on the
presence of shelfal agglutinated and calcareous benthic forami-
nifera, such as Lenticulina spp., and sediments dominated by
globular planktonic foraminifera including Hedbergella spp., Het-
erohelix spp. and Ticinella spp. Additional support for this is based
on a lack of carinate foraminifera within wells along the southern
New Guinea margin.
Although the Woniwogi Formation is assigned a Late Jurassic to
Early Cretaceous age (Pieters et al., 1983), the planktonic forami-
nifera listed above (recorded from the Woniwogi Formation in the
Kembelangan-1 well) indicate a restricted late Early Cretaceous,
Aptian-Albian, age.
4.8. Late Cretaceous
Relative sea-level rise reached its peak during the Late Creta-
ceous where water depths in excess of 100 m are interpreted across
much of western New Guinea (Fig. 9b). Many of the 58 reviewed
wells contain diagnostic deep-water taxa, dominated by carinate
globotruncanid planktonic foraminifera including, but not exclu-
sively, Abathomphalus mayaroensis, Dicarinella spp., Gansserina
gansseri, Globotruncana aegyptiaca, Globotruncana arca, Globo-
Fig. 8. Bathonian-Callovian aged ammonites collected from the Kopai Formation close truncana linneiana, Globotruncana ventricosa, Globotruncanita spp.,
to the village of Wendesi. A) Macrocephalites keeuwensis, B) Sphaeroceras boehmi and C) Globotruncanita stuartiformis, Helvetoglobotruncana helvetica, Mar-
Holcophylloceras indicum.
ginotruncana spp., Rosita spp., Rosita fornicata, Rotalipora spp.,
Rugoglobotruncana spp., Whiteinella spp., Whiteinella arche-
interpretation is validated further by widespread evidence of
ocretacea, and globular planktonic foraminifera including Hetero-
Middle Jurassic belemnites in sequences in Papua New Guinea,
helix spp., Pseudoguembelina spp. and Racemiguembelina fructicosa.
Papua/West Papua, the Sula Islands and Misool (Challinor, 1990).
Campanian to Maastrichtian age sediments were collected during
Additional evidence for marine conditions is provided by various
field work from the Imskin Limestone in the south-east of the Bird's
ammonites, bivalves and planktonic foraminifera from the Middle
Head (Fig. 9b). Six samples contain deep-water taxa, indicative of
Jurassic Tamrau Formation, found in the northern-most Bird's Head
outer neritic to lower bathyal water depths (>100 m). These include
(Pieters et al., 1983).
including Abathomphalus mayaroensis, Contusotruncana fornicata, C.
plummerae, Gansserina gansseri, Globotruncana arca, Globotruncana
4.6. Late Jurassic bulloides, Globotruncana linneiana, Globotruncanita conica, Globo-
truncanita. stuarti, Rugotruncana subcircumnodifer and Heterohelix
Continued regional transgression into the Late Jurassic saw the globulus (Fig. 10). The abundance of these carinate planktonic
seaway between the two landmasses of the former Sula Spur attain foraminifera in both wells and outcrop samples indicate deposition
water depths in excess of 100 m (Fig. 7f). The deltaic system to the within an upper bathyal setting, in water depths in excess of 300 m.
Fig. 9. Palaeogeographic reconstructions of western New Guinea, showing the paleogeographic evolution in the (a) Early Cretaceous; (b) Late Cretaceous; (c) Paleocene; (d) Early
Eocene; (e) Middle-Late Eocene, and the (f) Oligocene. These maps are based on the synthesis of biostratigraphic data and interpreted paleodepositional environments from public
domain well data, biostratigraphic reports, regional geology, sedimentological interpretations and new outcrop data. The number of data points used for each map are indicated in
each time slice (e.g. n ¼ ‘x’) and are shown as white dots. These data provide readers with some indication of our level of certainty for each reconstructions/region.
Fig. 10. Age-diagnostic Late Cretaceous planktonic foraminifera, and key palaeoenvironmental indicators, observed in outcrop samples. (aed) Carinate morphologies indicative of
water depths greater than 100 m. (eef) Globular planktonic foraminifera. Key - Globotruncana spp.(G), Contusotruncana fornicata (C.f), Globotruncana arca (G.a), Globotruncana
bulloides (G.b), Heterohelix globulus. (H.g).
4.9. Paleocene Five samples collected from the Imskin Limestone near Rum-
berpon Island were dated to be Paleocene age. All samples are
Following the Late Cretaceous relative sea-level high, water interpreted to have been deposited in an outer neritic to lower
levels receded during the Paleocene, particularly around the bathyal setting where water depths exceed 100 m (Fig. 9c). These
southern Bird's Head, Neck and Body (Fig. 9c). The distribution of samples contain a planktonic foraminiferal assemblage comprising
shallow water (<20 m) areas is delineated by the outcrop distri- globular and carinate morphologies including Acarinina coal-
bution of the Waripi Formation and where these sequences were ingensis, A. primitiva, Globanomalina imitata, G. ovalis, Morozovella
intersected in wells, particularly in the southern Bird's Body aequa, M. angulata, M. conicotruncata, Subbotina spp. and Turbeo-
(Fig. 9c). The Waripi Formation consists of a shallow-water lime- globorotalia compressa.
stone containing abundant oolites, miliolids and bryozoa (Visser
and Hermes, 1962; Brash et al., 1991). Farther north, particularly 4.10. Early Eocene
within the Bintuni Basin and offshore to the west, deeper waters in
excess of 100 m are encountered in many wells. These wells contain Relative sea-level fall continued into the Early Eocene and more
Daram Formation turbiditic material and carbonate mudstones shallow water areas developed within the central Bird's Head
comprising carinate and globular foraminifera. Foraminifera (Fig. 9d). The Faumai Limestone contains shallow water carbonate
include Morozovella spp., M. acuta, M. aequa, M. angulata, M. edgari, bank and shoal deposits and reefal facies (Pieters et al., 1983). This
M. inconstans, M. pseudobulloides, M. velascoensis, Acarinina spp., is supported by well data where shallow water areas up to 20 m in
Eugubina spp., Globanomalina spp. and Subbotina spp. We interpret depth are interpreted north of the Bintuni Basin in the southern
that the Daram turbidites in the central Bird's Head were deposited Bird's Neck and Body based on the presence of alveolinids including
from east to west along strike of a narrow submarine canyon Lacazinella spp. and Fasciolites spp. Moderate water depths be-
opening towards the west (Fig. 9c). An exception to this trend is tween 20 m and 50 m are interpreted from the Faumai Limestone of
provided by sandstones from the Daram Formation that outcrop on several wells and outcrop samples that contain alveolinids as well
Misool. These sequences contain the larger benthic foraminifera as abundant large, flat, rotaliine foraminifera such as Assilina spp.,
Lockhartia and Discocyclina which indicate water depths between Cycloclypeus spp., Discocyclina spp. and Operculina spp. Pieters et al.
20 m and 50 m during Paleocene to Early Eocene (Belford, 1991). (1983) proposed that the Faumai Limestone was deposited
between the Middle Eocene and Oligocene. However, the presence Peninsula (Fig. 9d). The Bintuni wells contain mixtures of Early
of alveolinids including Alveolina globosa, A. laxa, A. moussoulensis Eocene globular and carinate planktonic foraminifera including
and A. subpyrenaica, and larger benthics including Asterocyclina Morozovella spp., M. aragonensis, M. formosa, M. quetra, M. sub-
spp., Discocyclina ranikotensis, Cuvillierina spp. and Daviesina spp botinae, Acarinina spp., Acarinina nitida and Subbotina spp. Rocks
(Fig. 11). indicate that the Faumai Limestone must have to be as old collected from the Imskin Limestone and Early Eocene age clasts
as the Early Eocene (Ypresian), correlating to planktonic forami- within the Pleistocene conglomerate from the Wandaman Penin-
niferal zone E1 and Indo-Pacific letter stage ‘Ta2’ (Fig. 4). sula also suggest water depths greater than 100 m during the Early
Deeper water areas are interpreted to persist in the wells of the Eocene (Fig. 9d). Samples collected from these localities contain the
Bintuni Basin, from outcrop samples collected close to Rumberpon planktonic foraminifera Acarinina spp., Acarinina bulbrooki, A.
Island and from limestone clasts extracted from a Pleistocene decepta, Globigerina lozanoi, Globigerinatheka spp., Morozovella
conglomerate collected on the east coast of the Wandaman formosa, M. lensiformis, M. subbotinae and Subbotina spp (Fig. 11).
Fig. 11. Age-diagnostic Early Eocene foraminifera, and key palaeoenvironmental indicators, observed in outcrop samples. (aee) Large, flat, rotaliine foraminifera indicative of water
depths between 20 m and 50 m from the Faumai Limestone. (f) Globular planktonic foraminifera indicative of water depths between 50 m and 100 m, Imskin limestone. (geh)
Deep-water facies containing carinate planktonic foraminifera indicative of water depths in excess of 100 m, Imskin Limestone. Key - Alveolina spp. (A), Asterocyclina spp. (As),
Alveolina subpyrenaica (A.s), Alveolina moussoulensis (A.m), Discocyclina ranikotensis (D.r), Alveolina globosa (A.g), Planostegina spp. (O), Daviesina spp. (D), Nummulites spp. (N),
Acarinina spp. (Ac), Globigerinatheka spp. (Gt), Morozovella spp. (Mz).
4.11. Middle - Late Eocene developed to the south of the Bird's Neck (Brash et al., 1991;
Norvick, 2003), with deeper waters found to the northeast and
The lowest Paleogene relative sea-level occurred across much of west (Fig. 9f). This narrow island was surrounded by shallow bodies
western New Guinea during the Middle to Late Eocene (Fig. 9e). of water, denoted by the presence of Austrotrillina spp. in several
Shallow water areas were prevalent across the central Bird's Head wells including ASA-1X, ASF-1X and ASM-1X (Fig. 9f). Occasional
and Seram, and extended along the southern Bird's Neck and Body reefal build-ups are interpreted farther north where Nummulites
(Fig. 9e). These shallow waters are indicated by limestones domi- spp are recorded from TBE-1X (Fig. 9f). Water depths up to 50 m,
nated by Alveolina and Lacazinella (Visser and Hermes, 1962), while around the southern Bird's Head and Neck (Fig. 9f), are indicated by
deeper water deposition around the Bird's Neck is indicated by the presence of larger benthic foraminifera including Cycloclypeus
planktonic foraminifera collected from limestone clasts within a spp., Heterostegina borneensis, Operculina spp. and Pararotalia spp.
Plio-Pleistocene conglomerate exposure (Fig. 9e). Moderate water depths are also interpreted in the Salawati Basin,
Well data indicate the presence of shallow waters no greater primarily from well reports of Heterostegina borneensis (Visser and
than 20 m depth punctuated by isolated reefal build-ups across Hermes, 1962). Deeper water areas (Fig. 9f) occurred where
most of the central Bird's Head Peninsula (Fig. 9e). This is primarily Oligocene aged rocks, including those of the Sirga Formation, are
based on the presence of shallow water and reef-loving taxa such as dominated by intermediate water depth taxa such as Catapsydrax
Alveolina spp., Fasciolites spp., Lacazinella wichmanni, Nummulites spp., Globigerina ampliapertura, Globoturborotalita ouachitaensis,
spp., Nummulites djodjarkartae and Pararotalia spp. as well as corals Paragloborotalia opima recorded within the Klalin-1, and Onin
observed within the ASA-1X, Aum-1, Boka-1X, Rawarra-1, Sago-1, South-1X wells.
Sebyar-1 and TBE-1X wells. Bathymetric gradients away from the Six samples of Early and Late Oligocene age were collected from
shallow water platforms approach 50 m (Fig. 9e) where large flat the west coast of Cenderawasih Bay (Fig. 9f). Shallow water reef
rotaliines including Assilina spp., Discocyclina spp., Heterostegina front facies (<10 m water depth) were found near Rumberpon Is-
spp., Operculina spp. and assemblages of small calcareous benthic land where samples contain specimens of Neorotalia sp. and one of
foraminifera typical of shelf settings are found in wells East Misool- the last species of Nummulites, N. fichteli (BouDagher-Fadel, 2008).
1, Soeaboor-1, Steenkool-1 and Tarof-2. Deeper water (50e100 m) Late Oligocene rocks were also observed in sedimentary lenses of
facies are interpreted in the Onin exploration wells based on the the Arfak Volcanics of the eastern Bird's Head and Auwewa For-
presence of Acarinina spp., Globigerinatheka spp. and Morozovella mation on Supiori (Fig. 9f). These samples consist of planktonic
spp. foraminiferal packstones and wackestones indicating outer slope
Interpretations of biostratigraphic data within the exploration depths between 50 m and 100 m. Planktonic foraminifera of ‘in-
wells are supported by outcrop evidence along the western coast- termediate-water’ depths consist of globular morphologies
line of Cenderawasih Bay. Close to the village of Ransiki, shallow including Globigerina gortanii, Globigerina praebulloides, Globiger-
water facies include grainstones containing large Alveolina elliptica inoides primordius and Globoquadrina binaiensis. However, these are
and Nummulites gizehensis within samples of the Faumai Limestone found east of the Ransiki Fault (Fig. 2) and may indicate deeper
(Fig. 12). Farther to the south-east of Ransiki, samples contain large water depths away from the current setting and juxtaposed against
flat rotaliines including Assilina exponens, Asterocyclina sp. and more shallow water rocks through movement along this fault.
Discocyclina sella indicative of moderate water depths. Water
depths between 50 m and 100 m are interpreted close to Rum- 4.13. Oligocene-Miocene
berpon Island (Fig. 9e), where rocks of the Imskin Limestone
contain the planktonic foraminifera Acarinina intermedia, Globi- Towards the end of the Oligocene and beginning of the Miocene
gerina tripartita, Porticulasphaera mexicana and Subbotina spp. Parts arc-continent collision resulted in folding and thrusting of intra-
of the Imskin Limestone (including transported clasts within a Pacific island arc material as it was accreted to the Australian
conglomerate on the Wandaman Peninsula) indicate outer neritic continent (e.g. Davies et al., 1996; Hall, 2002; Wilson, 2002; Hill and
water depths in excess of 100 m around the Wandaman Peninsula Hall, 2003; Gold et al., 2014). Much of this material was exposed
region. Samples here contain a mixture of globular planktonic with up to 820 m of section being lost due to sub-aerial erosion.
foraminifera including Acarinina bullbrooki, A. decepta, A. pentaca- This is marked by a widespread angular unconformity (Gold et al.,
merata, A. primitiva, A. pseudotopilensis, Globigerinatheka sp., Sub- 2014) identified in several wells to the west of the Bird's Head
botina eocaenica and carinate forms including Morozovella Peninsula as well and as far as the eastern margin of Cenderawasih
aragonensis and M. crassata (Fig. 12). Bay (Fig. 13a).
The oldest foraminifera observed on the islands of Biak and
Supiori are Pellatispira sp. These are an exclusively Late Eocene 4.14. Early Miocene
(Priabonian) aged genus indicative of Indo-Pacific ‘letter stage’ Tb
(Adams, 1970, Figs. 4 and 12). These larger benthic foraminifera are The Early Miocene saw the presence of widespread shallow
found reworked within clasts of Auwewa Formation material water carbonate platforms across western New Guinea and Cen-
within the Batu Ujang Conglomerate outcropping around Wafor- derawasih Bay, with maximum water depths no greater than 50 m
dori Bay on the north coast of Supiori. Although reworked, Pella- (Fig. 13b). Early Miocene aged units of the New Guinea Limestone
tispira sp. signify moderate water depths up to several 10's of Group including the Kais, Koor and Maruni limestones on the Bird's
metres within the vicinity of Supiori. This taxon is also observed Head Peninsula, the Wurui Limestone of Yapen, and Wainukendi
within the Auwewa Formation encountered in wells in the Mam- and Wafordori formations of Biak and Supiori. These consist of
beramo region (located in the northern section of the Bird's Body, predominantly shallow water to reefal carbonates (Visser and
east of Yapen Island e this falls outside of the boundary of the maps Hermes, 1962; Pieters et al., 1983; Brash et al., 1991). These units
presented in Figs. 1, 2, 7 and 9). were mapped without distinction between shallow and relatively
deeper water facies; therefore the distribution of these formations
4.12. Oligocene is used only to interpret water depths no greater than 50 m
(Fig. 13b), thus accommodating potential heterogeneity within the
Relative sea-level rose across parts of western New Guinea New Guinea Limestone Group.
during the Oligocene. Despite this, a narrow terrestrial area The region was dominantly covered by shallow water during the
Fig. 12. Age-diagnostic Middle e Late Eocene foraminifera, and key palaeoenvironmental indicators, observed in outcrop samples. (aeb) Shallow water facies from the Faumai
Limestone. (ced) Shallow water facies observed in limestone lenses of the Auwewa Formation from Supiori. (eef) Globular planktonic foraminifera indicative of water depths
between 50 m and 100 m, Imskin Limestone. (h) Deep-water facies containing carinate planktonic foraminifera indicative of water depths greater than 100 m, Imskin Limestone.
Key e Nummulites gizehensis (N.g), Pellatispira spp. (Pt), Acarinina spp. (Ac), Globigerinatheka spp. (Gt), Acarinina pentacamerata (A.pe), Acarinina bullbrooki (A.b), Subbotina spp. (Sb),
Acarinina primitiva (A.pr), Daviesina spp. (D), Morozovella spp. (Mz).
Early Miocene e dominated by reefs and carbonate platforms Miogypsina spp., Miogypsinoides spp., Spiroclypeus spp. and other
(Fig. 13b). These carbonates have abundant larger benthic forami- organisms such as sponges, coral, echinoids and bivalves. This
nifera and they occur across much of western New Guinea, platform was surrounded by a body of water no greater than 50 m
including carbonate build-ups and patch-reefs in the Salawati Basin in depth (Fig. 13b) indicated by the presence of the larger benthic
(Gibson-Robinson and Soedirdja, 1986). foraminifera Operculina spp., Heterostegina spp. and Cycloclypeus
A broad platform populated by reefal build-ups extending from spp. Rare deeper water sediments of this age also occur in Seram
the western Bird's Head to the Bird's Body (Fig. 13b) was interpreted where they contain the globular planktonic foraminifera Globiger-
from 85 wells. These wells intersect packstones, grainstones and inoides spp., Globigerina spp. and Catapsydrax spp.
reefal rudstones and floatstones that contain shallow water taxa In outcrop, many reefal carbonates can be seen at the base of the
including Alveolinella praequoyi, Amphistegina spp., Austrotrillina Kais and Maruni Limestones of the mainland and Wainukendi
spp., Borelis spp., Flosculinella spp., Lepidocyclina spp., miliolids, Formation of Biak and Supiori. These reefs are mapped isolated
Fig. 13. Palaeogeographic reconstructions of western New Guinea, showing the paleogeographic evolution in the (a) Oligo-Miocene; (b) Early Miocene; (c) Middle Miocene; and (d)
Late Miocene. These maps are based on the synthesis of biostratigraphic data and interpreted paleodepositional environments from public domain well data, biostratigraphic
reports, regional geology, sedimentological interpretations and new outcrop data. The number of data points used for each map are indicated in each time slice (e.g. n ¼ ‘x’) and are
shown as white dots. These data provide readers with some indication of our level of certainty for each reconstructions/region.
patch reefs (Fig. 13b), although their lateral extent is unknown. Early Miocene shallow water carbonate platforms were replaced
Reefal carbonates and those deposited in moderate water depths by more moderate water depths in the Salawati and Bintuni basins,
contain an abundant and diverse fossil assemblage, predominantly and areas south of the Bird's Head Peninsula. At the same time,
comprising larger benthic foraminifera: Eulepidina badjirraensis, there is pronounced backstepping to shallow water regions to the
Lepidocyclina (Nephrolepidina) brouweri, L. (N.) isolepidinoides, L. north-east of the island of Supiori (Fig. 13c).
(N.) nephrolepidinoides, L. (N.) oneatensis, L. (N.) stratifera, L. (N.) A narrow moderate water depth carbonate platform developed
sumatrensis, Heterostegina borneensis, Miogypsina intermedia, M. on western and southern margin of Bird's Head Peninsula and the
kotoi, M. tani, Miogypsinoides bantamensis, Mdes. dehaarti, Miogyp- Bird's Neck (Fig. 13c). This broadly supports Brash et al. (1991)
sinodella primitiva, Miolepidocyclina, Operculina sp. and Spiroclypeus interpretation of platform carbonate in the southern margin of
tidoenganensis (Fig. 14). the Lengguru Fold and Thrust Belt and pelagic carbonates to the
northeast.
4.15. Middle Miocene Taxa indicative of moderate water depths, including Cyclo-
clypeus spp., Operculina spp., and Pseudorotalia spp., are prevalent
A regional transgressive event initiated in the Burdigalian so in 18 wells distributed across western New Guinea (Fig. 13c). Iso-
that by the Middle Miocene much of western New Guinea was lated carbonate platforms and occasional pinnacle reefs are recor-
submerged in water up to 100 m depth (Fig. 13c) (e.g. Brash et al., ded in the main basins of the Bird's Head Peninsula which contain
1991). Evidence for a rise in relative sea-level can be found in the shallow water taxa Alveolinella quoyi, Flosculinella bontangensis,
deep water facies of the Napisendi Formation and Sumboi Marl Lepidocyclina (N.) spp., Marginopora vertebralis, Miogypsina spp. as
found on the islands within Cenderawasih Bay, as well as in the well as corals, red algae, bivalves and echinoids. Deeper water areas
drowning successions at the top Maruni and Kais Limestone (Gold are interpreted from the presence of planktonic foraminiferal as-
et al., 2014). semblages including the taxa: Orbulina universa, Globigerina druryi,
Fig. 14. Age-diagnostic Early Miocene foraminifera, and key palaeoenvironmental indicators, observed in outcrop samples. (aed) Shallow water, reefal, grainstones of the Maruni
Limestone. (e) Shallow water packstone of the Kais Limestone. (f) Large, flat, rotaliines indicate water depths between 20 m and 50 m in the Maruni Limestone. Key e Lepidocyclina
(N.) sumatrensis (L.s), Lepidocyclina (N.) brouweri (L.b), Planorbulinella larvata (P.l), Spiroclypeus tidoenganensis (S.t), Eulepidina spp. (Eu), Miogypsina spp. (Mg), Amphistegina spp. (Am),
Heterostegina spp. (Hs).
Globigerinoides subquadratus, Globigerinoides diminutus, Globiger- L. (N.) omphalus, L. (N.) verbeeki, miogypsinids including Miogypsi-
inoides bisphaericus, Praeorbulina glomerosa, Praeorbulina tran- noides indica, Miogypsina cushmani, M. intermedia, M. kotoi, M.
sitoria, Paragloborotalia siakensis, Globorotalia fohsi. regularia (Fig. 15).
Outcrop samples of shallow water deposits from the Koor For-
mation in the northern Bird's Head Peninsula include soritid fora- 4.16. Late Miocene
minifera (e.g. Marginopora vertebralis) and miliolids including
Quinqueloculina spp. and Alveolinella quoyi. These sequences are Relative sea-level continued to rise during the Late Miocene so
also found on Biak where they are interbedded within the Napi- that water depths greater than 100 m were widespread across
sendi Formation. An isolated reef is interpreted near Rumberpon much of western New Guinea (Fig. 13d). Visser and Hermes (1962)
Island at this time (Fig. 13c) e samples from this area contain reef- and Golonka et al. (2006, 2009) interpret deep water facies rocks,
loving organisms such as miogypsinid and lepidocyclinid larger represented by the Befoor and Klasafet Formations of the Bird's
benthic foraminifera. Head and Neck, to indicate greater deep-water deposition across
Deep water deposits occur in the upper parts of the Kais and much of the region. Small reefal areas are present during this time,
Maruni limestones and Napisendi Formation, extending south to but cover much smaller areas than those seen during the Early
the central Bird's Head and Cenderawasih Bay (Fig. 13c). These Miocene (e.g. Visser and Hermes, 1962). However, wireline logs
samples contain abundant globular planktonic foraminifera that from exploration wells indicate these areas were probably depos-
indicate intermediate water depths between 50 m and 100 m. Ex- ited in slightly deeper water, particularly in the Salawati and Bin-
amples include Orbulina suturalis, O. universa, and many species of tuni basins, as has been recognised in several other studies
Globigerinoides including G. quadrilobatus, G. trilobus, and rare (Vincelette, 1973; Redmond and Koesoemadinata, 1976; Collins and
Globorotalia spp. (Fig. 15). Other outcrop samples from the Kais and Qureshi, 1977; Gibson-Robinson and Soedirdja, 1986). We also take
Maruni Limestones of the Bird's Head Peninsula and the Wafordori the Kais Limestones to be Early to Middle Miocene in age, rather
Formation on Biak contain large flat rotaliine foraminifera than these being as young as Late Miocene as per Norvick (2003).
including Katacycloclypeus annulatus and Cycloclypeus carpenteri, This discrepancy can explain why we do not show a widespread
lepidocyclinids including Lepidocyclina (N.) brouweri, L. (N.) ferreroi, shallow water carbonate platform through the centre of the Bird's
Fig. 15. Age-diagnostic Middle Miocene foraminifera, and key palaeoenvironmental indicators, observed in outcrop samples. (a) Large, flat, rotaliines indicating water depths
between 20 m and 50 m from the Maruni Limestone. (b) Shallow water wackestone containing taxa indicative of water depths no greater than 20 m. (ced) Globular planktonic
foraminifera indicating water depths between 50 m and 100 m from near the top of the Maruni Limestone. Key e Katacycloclypeus annulatus (K.a), Borelis melo (B.m), Globigerinoides
quadrilobatus (G.g), Orbulina universa (O.u).
Head and Neck in the Late Miocene (e.g.Norvick, 2003). Outcrop samples collected from the Befoor and Klasaman for-
Evidence for the prevalence of water depths between 50 m and mations in the eastern Bird's Head contain abundant globular
100 m in the eastern Bird's Head and islands to the north of Cen- planktonic foraminifera (e.g. many species of Globigerinoides spp.,
derawasih Bay come from the abundance of ‘intermediate-water’ Neogloboquadrina spp., Pulleniatina spp., Sphaeroidinella spp. and
species including Candeina nitida and Orbulina suturalis (Be , 1977) Sphaeroidinellopsis spp., as well as Orbulina universa). Carinate
found within the outcrop samples we examined. Farther south, in planktonic foraminifera such as species of Globorotalia spp. are
samples collected close to Rumberpon Island (Fig. 13d), water interpreted to have been washed into this environment and large
depths in excess of 100 m are interpreted from abundant carinate flat benthic foraminifera such as Operculina spp. are interpreted to
planktonic foraminifera (e.g. Globorotalia plesiotumida, Truncor- have been transported down slope. To the north-east of the Bird's
otalia ronda) and the thick-walled globular planktonics (e.g. Head, evidence for shallower reefal settings occur within reef front
Sphaeroidinellopsis subdehiscens and Globoquadrina dehiscens). facies rocks of the Wai Limestone containing Calcarina spengleri,
These water depths are interpreted from wells in the Salawati and Amphistegina spp. and abundant rodophyte red algae deposited in
Bintuni basins as well as within the Arafura Sea, due to the presence front of back-reef facies units (Fig. 16a). Shallow water facies,
of thick-walled and carinate planktonic foraminifera mentioned interpreted as back-reef lagoons, to the east of the Bird's Head
above as well as Dentoglobigerina baroemoensis, Globorotalia mer- (Fig. 16a) contain soritid foraminifera including Marginopora ver-
otumida, Neogloboquadrina acostaensis, Neogloboquadrina humerosa tebralis, small rotaliids including Quasirotalia guamensis. Delicate
and Sphaeroidinellopsis spp. corals and the dasycladacean green alga, Halimeda are also found in
the Early Pliocene specimens.
4.17. Early Pliocene On the islands of Biak and Supiori, a small bathymetric high is
interpreted to pass quickly from inner slope sediments into outer
The Early Pliocene consisted of dominantly open marine set- neritic settings, with steeply inclined slopes found around the peak
tings across western New Guinea during the Early Pliocene (Fig. 16a). Outer neritic sediments representing water depths in
(Fig. 16a). Water depths in excess of 50 m are recorded from wells excess of 100 m occur towards the Biak Basin to the south-west.
across western New Guinea that contain microfossils assemblages These sediments contain common carinate planktonic forami-
dominated by globular and carinate planktonic foraminifera nifera including Globorotalia conoidea, G. margaritae, G. menardii, G.
including Globigerina spp., Globigerinoides spp., Globorotalia spp., miocenica, G. tumida, G. sphericomiozea, Truncorotalia crassula and
Neogloboquadrina spp., Sphaeroidinella spp. and Sphaeroidinellopsis the thick walled globular planktonic foraminifera Sphaer-
spp. oidinellopsis seminulina. Carinate planktonic foraminifera observed
Relatively shallower water facies are recorded in wells to the in the Korem and Wardo formations are indicative of >100 m water
south and west of the Bird's Head (Fig. 16a). This includes shallow depths.
water facies such as grainstones, coral floatstones and back-reef
lagoonal wackestones that contain the taxa Ammonia spp., 4.18. Late Pliocene
Amphistegina lessonii, Calcarina spengleri, Heterostegina spp., Mar-
ginopora spp., Neorotalia calcar, Pararotalia spp., Peneroplis spp., Sea-level regression occurred in western New Guinea towards
Pseudorotalia spp. and miliolids. the end of the Early Pliocene, resulting in extensive shallow water
Fig. 16. Palaeogeographic reconstructions of western New Guinea, showing the paleogeographic evolution in the (a) Early Pliocene; (b) Late Pliocene, and (c) Pleistocene. These
maps are based on the synthesis of biostratigraphic data and interpreted paleodepositional environments from public domain well data, biostratigraphic reports, regional geology,
sedimentological interpretations and new outcrop data. The number of data points used for each map are indicated in each time slice (e.g. n ¼ ‘x’) and are shown as white dots.
These data provide readers with some indication of our level of certainty for each reconstructions/region.
areas especially to the west of the Bird's Head Peninsula (Fig. 16b). Mokmer and Manokwari formations) (Fig. 16c). This deposition was
This emergent area is responsible for the formation of the regional largely coeval with the deposition of the Ansus Conglomerate on
intra-Pliocene unconformity of Pairault et al. (2003) and Decker Yapen, which may indicate that parts of this island were subaerially
et al. (2009). exposed During the Pleistocene. The northern most sub-basins in
Deep water areas are interpreted based on the presence of Cenderawasih Bay became much deeper during this period and
globular and carinate planktonic foraminifera including Globigerina these are interpreted to be filled by pelagic carbonates comprising
spp., Globigerinoides spp., Globorotalia spp., Neogloboquadrina spp., planktonic foraminiferal packstones (Fig. 16c).
Sphaeroidinella spp. and Sphaeroidinellopsis spp. The distribution of Palaeogeographic interpretations suggest a southwest directed
relatively shallower areas are interpreted based on the presence of deepening trend across a broad carbonate platform no deeper than
large flat rotaliines including Cycloclypeus, Heterostegina spp., 50 m in water into the much deeper setting of Cenderawasih Bay
Operculina spp. and typical back reef or lagoonal taxa such as soritid (Fig. 16c). The presence of a carbonate platform attaining these
and miliolid foraminifera, coral, echinoids and bivalves. moderate water depths is indicated by common occurrences of the
larger benthic foraminifera Heterostegina spp., and globular
4.19. Pleistocene planktonic foraminifera including Pulleniatina obliquiloculata and
Globigerinoides quadrilobatus. Rocks interpreted to have been
The relative fall in sea-level that commenced in the Late Plio- deposited in reefal, shallow water settings up to 10 m in depth
cene continued into the Pleistocene and through to the present day comprise grainstones that contain abundant encrusting rodophyte
in western New Guinea. Several areas of the Bird's Head, Neck and red algae resilient to the brunt of high hydrodynamic energies.
Body were submerged beneath waters no greater than 50 m and Behind this, quiet waters of the back-reef are situated to the east of
localised areas were subaerially exposed close to the Salawati and the island and contain delicate bryozoa and branching corals of the
Bintuni basins (Fig. 16c) as a precursor to the present day topog- genera Acropora and Porites. Dasycladacean green algae, such as
raphy of New Guinea. Halimeda, are also common. The disintegration of algal needles may
The islands found to the north of Cenderawasih Bay (e.g. Biak, contribute towards the large amount of micrite in wackestones
Yapen, Supiori) record carbonate platform deposition in shallow deposited in this setting.
water as well as reefal facies and sedimentry breccia (e.g. the
5. Discussion 5.1.3. Cenozoic

The Paleocene landmass of Norvick (2003) in the Bird's Head is
5.1. Comparisons with previous palaeogeographic reconstructions hereby reinterpreted as an isolated shallow water region. This is
based on evidence from oolitic and bioclastic shoal limestones
Our paleogeographic reconstructions broadly support the pre- within the Waripi Formation of the Salawati Basin.
viously published works of Visser and Hermes (1962), Audley- Our reconstructions broadly support the Early Eocene inter-
Charles (1965, 1966), Vincelette (1973), Redmond and Koesoema- pretation of Brash et al. (1991) and Golonka (2009) which show
dinata (1976), Collins and Qureshi (1977), Gibson-Robinson and pelagic carbonate deposition in the Bird's Neck. This interpretation
Soedirdja (1986), Brash et al. (1991), Norvick (2003) and Golonka is supported by carinate planktonic foraminifera observed in
et al. (2006, 2009). However, there are a number of notable dif- outcrop samples from this region. By the Middle to Late Eocene, we
ferences, which we suspect are largely driven by access to addi- have interpreted widespread shallow water carbonate deposition
tional data, as well as a thorough, consistent re-interpretation of across the majority of western New Guinea, much like the earlier
regional biostratigraphic data. We summarise the main differences maps of Visser and Hermes (1962), Norvick (2003) and Golonka
between our work and earlier interpretations in the following (2009). Our reconstructions refine Visser and Hermes (1962)
sections. palaeogeographic interpretation of open marine facies close to
the Fakfak region of the Bird's Head Peninsula as well as near the
Wandaman Peninsula (Fig. 9e).
5.1.1. Paleozoic
The Oligocene reconstructions are broadly similar to those of
Visser and Hermes (1962) interpret paralic sediments across
Brash et al. (1991) and Norvick (2003), showing a terrestrial area in
much of western New Guinea during the Permo-Carboniferous
the southern Bird's Neck deepening towards the northeast. Norvick
(Fig. 7aeb). We interpret that terrestrial environments were more
(2003) interpret the central Bird's Head to be emergent at this time,
prevalent during the Carboniferous with increasing marine influ-
although evidence from outcrop samples indicates shallow water
ence developing in the early Permian. Our interpretation of broadly
deposition was occurring in this region (Fig. 9f). This was also
terrestrial settings during the Carboniferous is in contrast to the
recognised by Golonka et al. (2006, 2009).
interpretation of Golonka et al. (2006), who propose a deep-water
slope setting along the northern margin of New Guinea during this
5.2. Temporal trends
time. Visser and Hermes (1962) and Pieters et al. (1983) suggest
that the Aiduna Formation is the southerly equivalent to the 'C0
A first-order highstand sea-level occurred during the Silurian
Member of the Aifam Group to which they assign a Permian age.
(Ross and Ross, 1988; Golonka et al., 2006), but relative sea-level
However, Martodjojo et al. (1975) and Oliver et al. (1995) separate
fell between the Silurian and Devonian. The conditions changed,
the Aiduna Formation as a distinct lithological unit and assign a
with deep water deposition being replaced by dominantly
Carboniferous age based on biostratigraphy of the rugose corals.
terrestrial environments which persisted between the Permian
We favoured the biostratigraphic interpretation of Martodjojo et al.
and Early Jurassic (Fig. 17). Transgression throughout the Middle
(1975) and Oliver et al. (1995) for the age of this unit. In addition,
Jurassic and into the Cretaceous resulted in peak Mesozoic relative
we extend the Permian landmass of Audley-Charles (1965) farther
sea-level by the Late Cretaceous (Fig. 17). This period corresponds
north. This is based on Permian terrestrial sediments recorded from
with a time of maximum global sea-levels during the Phanerozoic
new wells drilled in this region north after 1965.
(Golonka et al., 2006), and the deposition of many fine-grained
siliciclastic formations. Relative sea-level dropped during the
5.1.2. Mesozoic Paleogene until the Middle to Late Eocene when widespread
Evidence from outcrop and well data also push the Australian- shallow water areas permitted the growth of extensive carbonate
New Guinea landmass and paralic sediments of Audley-Charles platforms represented by the oldest units of the New Guinea
(1966) farther north so that much of western New Guinea is Limestone Group. This includes the Faumai, Lengguru and Imskin
emergent during the Triassic (Fig. 7c). This supports palaeogeo- limestones as well as carbonate lenses within the Auwewa
graphic maps of Visser and Hermes (1962) and Norvick (2003) who Formation.
proposed land extended from the central Bird's Head, Neck and Supplementary video related to this article can be found at
southern margin of the Bird's Body (Fig. 7c). These interpretations http://dx.doi.org/10.1016/j.marpetgeo.2017.07.016.
contrast with Audley-Charles (1966) position of northern New Relative sea-level increased for a short duration during the
Guinea within a deep water setting at this time. Oligocene before the onset and perpetuation of arc-continent
Our reconstructions extend the deep-water settings of Audley- collision between the Australian and Pacific Plates between the
Charles (1966) along the central spine of New Guinea during the Oligocene and Early Miocene (e.g. Davies et al., 1996; Hall, 2002;
Late Jurassic. By the Early Cretaceous deep-water settings are Hill and Hall, 2003). This collision caused sub-aerial erosion of
interpreted across much of the Bird's Head. This differs from Paleogene sediments in some areas forming a regional Oligocene-
Norvick (2003) who place an isolated landmass within the central Miocene unconformity (Gold et al., 2014, Fig. 13a). This uplift is
Bird's Head at this time. also recognised as widespread carbonate platform growth and
Widespread open marine and bathyal facies across western New deposition of Early Miocene units of the New Guinea Limestone
Guinea during the Late Cretaceous support interpretations of Visser Group in other areas.
and Hermes (1962), Audley-Charles (1966), Brash et al. (1991) and Stable shallow-water carbonate deposition of the New Guinea
Norvick (2003). However, Brash et al. (1991) and Norvick (2003) Limestone Group continued for at least 6 Ma across much of
indicate that the late Campanian Ekmai sandstones of the Bird's western New Guinea until a second regional transgressive event
Neck were deposited in shallow water. This is based on the pres- initiated in the Burdigalian (Fig. 17). Relative sea-level rise reached
ence of larger benthic foraminifera Lepidorbitoides and Pseudorbi- its peak in the Late Miocene, possibly correlating with the global
toides found within the sandstones (Visser and Hermes, 1962). We Tor1 flooding event (Hardenbol, 1998; Gradstein et al., 2012;
speculate that the juxtaposition of Late Cretaceous deep- and Baillard et al., 2017), resulting in the deposition of widespread
shallow-water facies may be associated with shortening of the deep-water limestones and fine-grained siliciclastics of the Klasafet
Lengguru Fold and Thrust Belt. and Klasaman formations (Fig. 17). We also speculate that this may
Fig. 17. Relative sea-level curve for western New Guinea based on average bathymetry calculated from reinterpreted well data compared to global sea-level curves of Haq and Al-
Qahtani (2005), Müller et al. (2008), Snedden and Liu (2010) and Miller et al. (2011). Two main transgressive-regressive cycles are interpreted with peak relative sea-level occurring
during the Late Cretaceous and Late Miocene. Error bars ¼ standard error of the mean. The regional releative sea-level curve can also be viewed alongside the paleogeographic maps
in an animation in Supp. Data 2.
have been related to a phase of crustal extension associated with 5.3. Comparisons with computer models
the metamorphic core complexes exposed on the Wandaman
Peninsula (e.g. Bailly et al., 2009; François et al., 2016). Relative sea- Our palaeogeographic reconstructions broadly support, and
level began to fall again during the Pliocene (Fig. 17), culminating in build upon, previously published palaeogeographic maps of New
short-lived sub-aerial exposure of an area to the west of the Bird's Guinea based on empirical data (e.g. Visser and Hermes, 1962;
Head forming a regional intra-Pliocene unconformity (Pairault Audley-Charles, 1965, 1966; Brash et al., 1991; Golonka et al.,
et al., 2003; Decker et al., 2009). 2006, 2009) but differ to computer modelled global and regional
The regional Bird's Head relative sea-level curve is similar to palaeogeographies (e.g. Zahirovic, 2014, 2016; Heine et al., 2015;
that of published global sea-level curves (Haq and Al-Qahtani, Leprieur et al., 2016). Most of these models use global eustatic
2005; Müller et al., 2008; Snedden and Liu, 2010) from the Silu- sea-level curves (Haq et al., 1987, 2014; Haq and Al-Qahtani, 2005;
rian to Paleocene (Fig. 17). This implies that the primary control on Haq and Shutter, 2008; Müller et al., 2008; Snedden and Liu, 2010;
relative sea-level change throughout this time is eustatic. However, Miller et al., 2011) as a basic parameter, applying a particular sea-
there are disparities between the regional and global sea-level level curve(s) to regional basins, including those in Southeast
curves from the Early Eocene to Oligocene (Fig. 17). This suggests Asia. The sea-level curves of Haq et al. (1987) and Haq and Al-
that the primary control on relative sea-level change is more Qahtani (2005), in particular, are based on observations from the
localised at this time and may be attributed to tectonic effects of Arabian platform which has been a relatively stable homoclinal
regional subsidence and uplift and/or environmental controls carbonate ramp since the Paleozoic (Haq and Al-Qahtani, 2005).
influencing sedimentation rates. Following arc-continent collision This region therefore preserves a good record of facies changes up
in the Early Miocene the regional relative sea-level curve of western and down the ramp enabling the determination of past regional
New Guinea returns to recording the signal of global eustatic sea- sea-level change. Active plate margins however are less stable,
level change (Fig. 17). which is perhaps why we record different palaeogeographic
histories to the more automated/data mining approaches employed (15-5 Ma) (Leprieur et al., 2016). Leprieur et al. (2016) remark that
in some of the numerical models generated for New Guinea (e.g. ecological diversification is controlled by the availability of tropical
Zahirovic, 2014, 2016; Heine et al., 2015; Leprieur et al., 2016). reef habitat through time. However, our models show that car-
Heine et al. (2015) concluded that calculations of land areas bonate platforms flourished during the Middle-Late Eocene in
relative to the total area of continental crust extracted from the western New Guinea (Fig. 9e). We therefore suggest that tropical
empirical data of Smith et al. (1994) and Golonka et al. (2006) reef habitats were available since at least the Eocene, much earlier
produced palaeoshoreline maps that matched the sea-level than Leprieur et al. (2016) proposed. We speculate that the wide-
curves of Haq and Al-Qahtani (2005) and Müller et al. (2008). Yet, spread carbonate platform development in western New Guinea
the Smith et al. (1994) and Golonka et al. (2006) models have a during the Eocene may be controlled by regional tectonism and/or
sparse data coverage across Southeast Asia, with no data points for favourable environmental conditions that permitted high rates of
New Guinea or Indonesia (apart from Kalimantan). Therefore, carbonate production.
subtle regional deep marine incursions and the development of Although our palaeogeographic reconstructions do record
widespread carbonate platforms are not recorded in palaeogeo- changes in the long-term eustatic sea-level signal for the Paleozoic
graphic reconstructions. Leprieur et al. (2016) take a different and Mesozoic, these deviate from published curves from the
approach to mapping the development of carbonate platforms in Paleogene and Neogene (Fig. 17). Where the long-term eustatic
Southeast Asia by using a mechanistic model of species diversifi- trend records a fall in sea-level from the Late Cretaceous to Oligo-
cation combined with a model of synthetic paleobathymetry esti- cene; our relative sea-level curve suggests a minor regional trans-
mates to map the global spatial distribution of biodiversity hotspots gression between the Eocene and Oligocene (Fig. 17). Zahirovic et al.
since the Cretaceous. This approach models the migration of new (2016) and Yang et al. (2016) suggested widespread flooding of the
species and biodiversity hotspots through time, moving eastward Sundaland platform occurred during the Eocene. Yet, this rise in
from western Tethys through the Arabian Peninsula and Indian relative sea-level occurred at a time of global eustatic sea level fall
Ocean, eventually arriving in the Indo-Pacific during the Miocene (Haq and Al-Qahtani, 2005; Müller et al., 2008; Snedden and Liu,
Fig. 18. Maps showing where sections of the stratigraphic record have been removed at particular time slices. This includes during the: (a) Early Pliocene; (b) Oligo-Miocene; (c)
EarlyeMid Jurassic; (d) Triassic; (e) Late Permian, and (f) DevonianeCarboniferous.
2010; Heine et al., 2015). Yang et al. (2016) proposed the mecha- and Late Miocene. These coincide with peak transgressions shown
nism for this was to due dynamic topographic effects. Following in our palaeogeographic reconstructions. We interpret these hia-
continuing global sea-level fall in the Oligocene, many published tuses to represent drowning unconformities on the opposite end of
curves indicate a rise in sea-level from the Early Miocene (Fig. 17). the relative sea-level cycle to sub-aerial unconformities (e.g.
This contrasts to our curve which records localised sea-level fall, Schlager, 1981, 1989; 1999). These types of unconformity are prone
interpreted here to be caused by arc-continent collision between to forming condensed sections (Schlager, 1989) where basinal areas
New Guinea and intra-Pacific island arcs between the Oligocene are starved of sediment, thus producing a stratigraphic break in
and Early Miocene resulting in localised uplift and halting the well successions. Little is known about the Late Cretaceous event,
regional transgression of the Oligocene. Our regional relative sea- but recent work has shown that the Late Miocene drowning un-
level curve for western New Guinea again records the global conformity is related to the Middle to Late Miocene drowning of the
eustatic signal of sea-level rise throughout the Middle and Late widespread New Guinea Limestone Group carbonate platform
Miocene, followed by sea-level fall to present day levels (Fig. 17). (Gold et al., 2014).
These examples reinforce the point that global sea-level curves are
not typically appropriate for regions such as Southeast Asia, where 6. Conclusions
complex tectonism and favourable environmental conditions for
carbonate production are likely have a greater control on the Empirical data from well and outcrop samples from Carbonif-
palaeogeography than eustatic factors. Computer modelled palae- erous to Recent sediments were used to reinterpret the paleogeo-
obathymetries (e.g. Müller et al., 2008) are often too coarse to be graphic evolution of western New Guinea and to examine the long-
used as parameters to model subtle changes in palaeogeography at term regional record of sea-level change. We also showed that the
a regional scale. These models have the capability of computing use of empirical data to generate such maps, should lead to more
global bathymetric changes in hundreds to thousands of metres robust documentation of regional changes in relative sea-level than
water depth, however the use of palaeontological and sedimento- semi-automated modelling methods that primarily rely on global
logical data, as shown by this study, can model changes in ba- eustatic sea-level curves. In western New Guinea, relative sea-
thymetry at a scale from a few tens to hundreds of metres. levels were highest during the Late Cretaceous and Late Miocene.
Therefore, we propose that bathymetric models generated from These peaks correspond with those identified in long-term eustatic
local observational data sources allow for much more robust re- sea-level change. However, from the Eocene to Oligocene the
constructions of regional palaeogeographies for plate margins than relative sea-level curve deviates from the long-term global eustatic
models that primarily rely on global eustasy curves. The challenge sea-level. We attribute this change to regional tectonism and/or
lies in developing representative relative sea-level curves from the environmental factors, such as higher atmospheric and sea-water
available data sources and to use these to test and further develop temperatures that may have facilitated greater carbonate produc-
more regional to global models. tion. If we consider that the latitude and position of New Guinea
relative to Australia has not changed considerably since the Triassic
5.4. Unconformities then our palaeogeographic reconstructions south of the Australia-
Pacific suture from the Triassic onwards are relatively robust. The
Eight major unconformities are recognised across western New palaeoenvironmental interpretations of the post-collisional stra-
Guinea according to new biostratigraphic data as well as analyses of tigraphy of the region are also quite robust, however, these do not
well logs and existing literature. Six of these unconformities are account for any deformation associated with the interaction be-
interpreted as sub-aerial unconformities as they are supported by tween the Pacific and Australian plates, which is something that we
evidence for terrestrial deposition in our palaeogeographic re- will address in future.
constructions (Figs. 7, 9, 13 and 16). Where many wells do not
contain evidence for terrestrial deposition, they instead exhibit a Acknowledgments
stratigraphic break that records a period of non-deposition and/or
erosion. The areas of non-deposition and/or erosion identified This work was supported by the Southeast Asia Research Group
within the reviewed well data are depicted in Fig. 18. The oldest at Royal Holloway, funded by a consortium of oil companies. We
sub-aerial unconformities occur above the Kemum Formation at thank our fieldwork counterparts from the Institut Teknologi
the Devonian and Carboniferous boundary as well as during the Bandung as well as John Decker, Phil Teas, Angus Ferguson and
Late Permian. These unconformities reflect predominantly terres- Farid Ferdian (all previously of Niko Asia), together with the crew of
trial deposition of the Aifam Group during the Carboniferous. the Shakti live-aboard vessel for assistance during fieldwork. We
Similarly the Triassic and Early Jurassic unconformities are related would particularly like to thank Benjamin Jost and Max Webb for
to widespread terrestrial deposition of the Tipuma Formation. commenting on an earlier version of this manuscript.
Where terrestrial sediments do not accumulate, are not preserved,
or have been eroded, parts, or all, of the Carboniferous and Triassic- Appendix A. Supplementary data
Jurassic successions are missing.
Further sub-aerial unconformities are interpreted to occur at the Supplementary data related to this article can be found at http://
Oligocene-Miocene boundary, observed above the Sirga Formation, dx.doi.org/10.1016/j.marpetgeo.2017.07.016.
and during the Pliocene (Fig. 18). The Oligo-Miocene sub-aerial
unconformity is interpreted to be related to be related to uplift References
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Marine and Petroleum Geology 86 (2017) 1133e1158

Contents lists available at ScienceDirect

Marine and Petroleum Geology

Relative sea-level change in western New Guinea recorded by regional

1. Introduction numerous tectono-thermal events during the Paleozoic, Mesozoic

abruptly terminated platform accumulation (Brash et al., 1991;

This paper presents the results of several ﬁeld campaigns con-

west of the northern landmass is interpreted to persist into the Late

4.7. Early Cretaceous

By the Early Cretaceous, formerly subaerially exposed regions of

4.8. Late Cretaceous

5. Discussion 5.1.3. Cenozoic

Timor region. Palaeogeogr. Palaeoclimatol. Palaeoecol. 1, 297e305. pp. 491e514. IPA-G-139.

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