The Geological Society of AmericaSpecial Paper 487
2012
Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia
Benjamin ClementsStatoil ASA, Svanholmen 6, N-4033 Stavanger, Norway
Inga SevastjanovaRobert Hall
SE Asia Research Group, Department of Earth Sciences, Royal Holloway University of London, Egham, Surrey TW20 0EX, UK
Elena A. BelousovaWilliam L. Griffi nNorman Pearson
GEMOC ARC National Key Centre, Department of Earth and Planetary Sciences, Macquarie University, Sydney, NSW 2109, Australia
ABSTRACT
Detrital zircon U-Pb geochronology can make an extremely valuable contribu-tion to provenance studies and paleogeographic reconstructions, but the technique cannot distinguish grains with similar ages derived from different sources. Hafnium isotope analysis of zircon crystals combined with U-Pb dating can help make such distinctions. Five Paleogene formations in West Java have U-Pb age populations of 80–50 Ma (Late Cretaceous–Paleogene), 145–74 Ma (Cretaceous), 298–202 Ma (Permian–Triassic), 653–480 Ma (mid-Neoproterozoic–latest Cambrian), and 1290–723 Ma (late Mesoproterozoic–early Neoproterozoic). Hf-isotopes have been analyzed for 311 zircons from these formations. Differences in zircon U-Pb age and Hf-isotope populations refl ect changing sources with time. Late Cretaceous and Paleogene zir-cons are interpreted as having been derived from two temporally discrete volcanic arcs in Java and West Sulawesi, respectively. The Java arc was active before micro-continent collision, and the W Sulawesi arc developed later, on newly accreted crust at the SE Sundaland margin. The collision age is estimated to be ca. 80 Ma. U-Pb age and 176Hf/177Hfi characteristics allow a distinction to be made between Cretaceous granitic and volcanic arc sources. Zircons that are older than ca. 80 Ma have a conti-nental Sundaland provenance. Mid-Cretaceous zircons in all upper Eocene and lower Oligocene formations were derived from granites of the Schwaner Mountains of SW Borneo. Permian–Triassic zircons were derived predominantly from granites in the SE Asian Tin Belt. 176Hf/177Hfi ratios permit distinction between Tin Belt granites in the Main Range and Eastern Provinces, and indicate that only the lower Oligocene
Two percent of all global land area is situated in SE Asia, and it is estimated to yield 20%–25% of the sediment supplied to the world’s oceans (e.g., Milliman et al., 1999). This tropi-cal, tectonically active region with its deep Cenozoic basins (up to 15 km in the Malay Basin, Petronas, 1999) and high sedi-ment yield is therefore the ideal natural laboratory for interpret-ing detrital sedimentary processes. Today, large rivers, such as the Red, Mekong, and Irrawaddy, transport huge volumes of sediment from the India-Asia collision zone through Indochina to the Asian coast (e.g., Ludwig and Probst, 1998; Robinson et al., 2007). Similar sedimentary pathways from the Hima-layan orogen have been inferred for sediment transported to Cenozoic basins in SE Asia, particularly those that surrounded Borneo during the Paleogene (e.g., Hutchison, 1996; Métivier et al., 1999). However, recent regional tectonic (e.g., Hall, 2002, 2009a, 2009b; Hall et al., 2009) and provenance (van Hattum, 2005; van Hattum et al., 2006; Hall et al., 2008) studies indicate that the impact of the India-Asia collision across SE Asia was more subtle than that proposed by “indentor-style” models (e.g., Tapponnier et al., 1982; Replumaz and Tapponnier, 2003). The Paleogene strata of the circum-Borneo basins (e.g., the Crocker Fan in NE Borneo) have, instead, a local (SW Borneo and Thai-Malay Peninsula) SE Asian provenance (van Hattum et al., 2006; Hall et al., 2008).
Detrital zircon U-Pb geochronology is one of the most rewarding techniques used for provenance and paleogeographic reconstructions (e.g., Kröner and Şengör, 1990; Sircombe and Freeman, 1999; Fedo et al., 2003; Cawood et al., 2003, 2007; Gehrels et al., 2006; van Hattum et al., 2006; Stevens et al., 2010; Hietpas et al., 2011; Leier and Gehrels, 2011). This approach identifi es characteristic detrital zircon age clusters and matches them with potential source rock ages. It has been successfully employed for tracing sediment pathways, recording denudation histories, dating volcano-magmatic events, and identifying previ-ously unknown continental crustal fragments in many parts of the world, including SE Asia (e.g., Gehrels et al., 2003; Nemchin and Cawood, 2005; van Hattum et al., 2006, Smyth et al., 2007, 2008; Clements and Hall, 2008; Davis et al., 2010; Mange et al., 2010). However, in geologically complex settings, the ages of zircon populations derived from different source areas may be statistically indistinguishable (e.g., Howard et al., 2009; Davis et al., 2010). In such instances, U-Pb dating of detrital zircon is of limited value, unless supplemented by other lines of evidence. Hf-isotope analyses augment U-Pb data by providing insights
into the character and age of each zircon’s parental magma (e.g., Belousova et al., 2006). Similar information can also be obtained from whole-rock studies of the Sm-Nd isotopic system, which behaves similarly to the Lu-Hf isotopic system during most mag-matic processes (e.g., Patchett and Tatsumoto, 1980; Blichert-Toft and Albarède, 1997; Blichert-Toft et al., 1999; Vervoort and Blichert-Toft, 1999). However, 176Hf/177Hf
i ratios are less vari-
able than 143Nd/144Nd ratios in the mantle, giving a more robust background for interpretation of Hf-isotope data (e.g., Vervoort and Blitchert-Toft, 1999). The high concentrations of Hf and low Lu/Hf in zircon, and the resistance of most zircon grains to abra-sion or alteration during transport, make zircon a highly robust recorder of the Hf-isotope composition of its magmatic host rock. Therefore, combined zircon U-Pb and Hf-isotope studies of zir-con have resulted in detailed crustal-evolution models (Bodet and Schärer, 2000; Griffi n et al., 2004; Griffi n et al., 2006a; Murgulov et al., 2007; Bahlburg et al., 2010; Belousova et al., 2006, 2010; Kuznetsov et al., 2010; Matteini et al., 2010) and sedimentary provenance interpretations (e.g., Veevers et al., 2006; Belousova et al., 2009; Howard et al., 2009; Koglin et al., 2010; Zhou et al., 2011; Fanning et al., 2011).
In this paper we report U-Pb ages and Hf-isotope composi-tions of detrital zircons from West Java that record broad-scale sediment pathways and fl uxes across southern Sundaland (Fig. 1) during the Paleogene. Five formations with middle Eocene to early Oligocene depositional ages record the dispersal of silici-clastic detritus during the waning stages of Cretaceous to Eocene regional uplift and the elevation of Sundaland (the area of con-tinental crust extending SE from Indochina, including Sumatra, Borneo, Java, and the shallow seas between them [Fig. 1]). This study also gives insights into the evolution of Late Cretaceous and early Paleogene volcanic arcs and the timing of microcon-tinent collision at the Java margin, and demonstrates sediment recycling from the SE Asian basement and perhaps sedimentary rocks that were initially deposited in basins that formed in eastern Gondwana. This is the fi rst study to apply “in situ” detrital zircon U-Pb dating and Hf-isotope analyses to provenance studies in the SE Asian region.
GEOLOGICAL SETTING
The SE Asian region is tectonically complex and bordered by subduction zones that are characterized by intense seismic-ity and volcanism. The region comprises numerous fragments of continental crust, ophiolitic suture zones that were once oceanic basins, ancient and active volcanic arcs, and young ocean basins.
Cijengkol Formation contains signifi cant input from the Main Range Province, sug-gesting a partial change in drainage pattern. Older zircon ages are more diffi cult to interpret but probably record contributions from allochthonous basement and sedi-mentary rocks that were deposited prior to rifting of continental blocks from Gond-wana in the early Mesozoic.
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 39
Figure 1. Major features of the southern part of the Sunda Shelf. Bathymetry is from Sandwell and Smith (1997). Acidic volcanic and plutonic rocks of ages that correspond to age clusters discussed in this chapter are shown. Inset shows West Java; black boxes correspond to the Ciletuh Bay (A), the Bayah Dome (B), the Sukabumi area (C), and the area around Padalarang (D). Black triangles are Holocene volcanoes.
SUMATRA
JAVA
PENINSULARMALAYSIA
BANGKA
BILLITON
SCHWANERMOUNTAINGRANITES
TIN-BELTGRANITES
BORNEO
SUNDALAND Approximate boundary between Cretaceous & older continental crust and Cretaceous melange
100°E 105°E 110°E 115°E
0°
5°S
5°N
Edge of Sundaland(Hamilton, 1979)
Bandung
A
BC
Jakarta
WEST JAVA
PadalarangMalingping
Bayah
D
28A
30A
8A
13B
2C
22D
4B
1000 m
1000 m
1000 m3000 m
3000 m
1000 m
5000 m
5000 m
BALI
100 m
kilometers
0 100 300 400 500200
Upper Cretaceous granitic & volcanic rocks
Lower Cretaceous granitic & acid igneous rocks
Main Range: Triassic granites
Eastern Province: Permian and Triassic granites
Variable age (203-5 Ma)granites and arc rocks
BORNEO
MALAY PENINSULA AND SUMATRA
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The entire region is allochthonous and has developed predomi-nantly by the addition of continental fragments to the active mar-gins (Hall, 2008). The majority of these continental fragments were derived from Gondwana (e.g., Şengör, 1979; Audley-Charles, 1983; Metcalfe, 1988, 1996), and this SE Asian “core” is referred to as Sundaland. Sundaland includes the Indochina–East Malaya and Sibumasu blocks, which separated from Gond-wana in the Paleozoic. Indochina–East Malaya separated from Gondwana in the Devonian and amalgamated with the South and North China blocks, forming the composite Cathaysia block in the Early Carboniferous (Metcalfe, 2009), whereas Sibumasu separated in the Permian and was part of Sundaland by the Early Triassic (Barber and Crow, 2009; Metcalfe, 2009). Two other continental Gondwana-derived blocks—SW Borneo (Banda) (Hall, 2009b; Hall et al., 2009) and E Java–W Sulawesi (Argo) (Smyth et al., 2007; Hall et al., 2009)—were subsequently added to the core of Sundaland in the Mesozoic.
In the Early Cretaceous, Sundaland was broadly in its pres-ent position, with subduction at its western, southern, and eastern margins. Subduction beneath Sundaland ceased in the Late Creta-ceous after the addition of microcontinental fragments at the Java margin (e.g., Smyth et al., 2007; Hall, 2009b; Hall et al., 2009). From the Late Cretaceous to ca. 45 Ma the margin was inactive (Hall et al., 2009; Hall, 2008) and much of Sundaland was emer-gent (Hall and Morley, 2004; Clements et al., 2011). As a conse-quence of this regional elevation, almost no sedimentary rocks of Late Cretaceous–early Paleogene age are preserved in the region. Little is known about the Late Cretaceous and early Paleogene paleogeography and paleodrainage in Sundaland. At ca. 45 Ma subduction recommenced (Hall, 2009b) and sediments started to accumulate within the Sundaland interior and at the continental margins. During the late Eocene and Oligocene, thick siliciclas-tic strata were deposited across the region (e.g., Polachan et al., 1991; Doust and Noble, 2008; Smyth et al., 2008).
SUNDALAND GEOLOGY AND POTENTIAL SEDIMENT SOURCES
Most of the Sundaland region is underlain by heterogeneous Precambrian metamorphic basement that is poorly exposed and typically poorly dated. Traditionally it was assumed that in the Malay Peninsula, basement rocks included Precambrian gneisses, marbles, schists, and phyllites overlain by Cambrian to Permian sedimentary rocks (Metcalfe, 1988). However, high-grade schists and granulites exposed, for example, in Indochina (e.g., the Kon-thum massif in central Vietnam, the Doi Inthanon Metamorphic Complex in Thailand, etc.) that were previously assumed to be Archean (e.g., Baum et al., 1970; Hutchison, 1989) are now known to be much younger and yield Paleozoic, Mesozoic, and Cenozoic isotopic ages (e.g., Carter et al., 2001; Nagy et al., 2001; Nam et al., 2001). Hf-isotope data for detrital zircon and baddeleyite (Bodet and Schärer, 2000) and Nd-isotope studies (Lan et al., 2003) from Indochina suggest that the basement is no older than 2.4–2.5 Ga beneath this area. Sevastjanova et al.
(2011) demonstrated through U-Pb and Hf-isotope studies of zir-con dating that the basement beneath the Malay Peninsula is pre-dominantly Paleoproterozoic (1.9–2 Ga beneath Sibumasu, and 1.7–2 Ga beneath East Malaya), probably with minor Archean components (ca. 2.7–2.8 Ga). U-Pb ages of inherited zircon and Nd model ages (T
DMNd) of granitoids also suggest the presence of
Proterozoic basement beneath the Malay Peninsula (Liew and McCulloch, 1985; Cobbing et al., 1992). In Sumatra, schists and gneisses that are exposed in the northwest are considered to represent a pre-Carboniferous basement (Barber and Crow, 2005), and elsewhere, continental basement is inferred from the presence of ignimbrites and granites of varying ages. The old-est sedimentary rocks are Carboniferous and consist of tillites, limestones, sandstones, and shales. Granitoids from the islands of Bangka and Belitung yield Proterozoic (1.0–1.8 Ga) T
DMNd
(Cobbing et al., 1992). In Borneo, the isotopically undated meta-morphic Pinoh Group is suggested to be Carboniferous–Permian or older (Amiruddin and Trail, 1993; de Keyser and Rustandi, 1993; Pieters and Sanyoto, 1993). However, most of the island is composed of ophiolitic, island arc, and microcontinental crust accreted during the Mesozoic (Hamilton, 1979; Hutchison, 1989; Metcalfe, 1996; Hall et al., 2008, 2009).
Late Paleozoic–early Mesozoic subduction of Paleo-Tethys oceanic crust and collision of continental fragments in central Sundaland (Thailand, the Malay Peninsula, and Sumatra) were accompanied by a major period of granitoid intrusion (e.g., Hutchison, 1977; Cobbing et al., 1992; Metcalfe, 2000). This was initially associated with subduction preceding collision, and later with post-collisional thickening of the continental crust (Hutchi-son, 1989, 1996) and emplacement of granitoids into the suture zone (Barber and Crow, 2009; Sevastjanova et al., 2011). As a result, there are many Permian and Triassic tin-bearing granitoids in the region (Fig. 1) (Bignell and Snelling, 1977; Beckinsale et al., 1979; Liew and Page, 1985; Seong, 1990; Krähenbuhl, 1991; Cobbing et al., 1992). Most of these granitoids form part of the SE Asian Tin Belt, which extends from Myanmar through the Thai-Malay Peninsula into the Indonesian Tin Islands (Fig. 1). Minor Jurassic and abundant Lower Cretaceous plutonic and volcanic rocks (exposed in Sumatra, SE Borneo, and Sulawesi) are also commonly interpreted as subduction-related and post-collisional. These typically occur inboard of a zone of arc-related and ophiolitic subduction complexes (accreted to the margin in the early Late Cretaceous), and high-pressure, low-temperature, subduction-related metamorphic rocks. Cretaceous granites are known from the currently submerged Sunda Shelf (Hamilton, 1979) and the Schwaner Mountains of SW Borneo (e.g., Wil-liams et al., 1988; van Hattum et al., 2006) as well as smaller occurrences in Sumatra (Cobbing, 2005), the Central Belt of the Malay Peninsula (Cobbing et al., 1992) and Thailand (Cobbing et al., 1992). In contrast to the abundant evidence for Jurassic and Cretaceous subduction in the region, there is little evidence for subduction-related volcanism during the Late Cretaceous and Paleocene, except in parts of West Sulawesi (van Leeuwen, 1981; Hasan, 1990; Elburg et al., 2002) and Sumba (Abdullah et al.,
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 41
2000). The paucity of plutonic and volcanic rocks of Late Creta-ceous to early Eocene age throughout the region is interpreted to represent a period of subduction quiescence (Hall, 2009b).
STRATIGRAPHY
The ages of sedimentary fi ll in many of the basins through-out Sundaland vary only slightly, and they share characteristics that indicate a similar Cenozoic history and tectono-stratigraphic development. In all instances, basins overlie older rocks with a profound unconformity, and Upper Cretaceous and Paleocene strata in the region are almost entirely absent (Clements et al., 2011). Sedimentary rocks above the unconformity are Eocene and younger, and many are terrestrial and were deposited across the region in extensional half-graben basins, and at the Sundaland continental margins. The sedimentary record for the Cretaceous and early Paleogene, however, has largely been lost, although the oldest deposits above the unconformity, deposited through-out much of Sundaland, including West Java, provide a reworked record of the broad-scale sediment fl uxes that typifi ed the Late Cretaceous to Paleocene regional elevation of Sundaland.
Middle Eocene
In West Java, middle Eocene rocks (van Bemmelen, 1949; Schiller et al., 1991; P. Lunt, 2006, personal commun.; Clem-ents, 2008) are exposed in the Ciletuh Bay area (Fig. 1). These are the Ciletuh and Ciemas Formations (Clements and Hall, 2007) (Fig. 2 and Table 1) and represent the oldest sequences above basement (Fig. 2).
The Ciletuh Formation consists of coarse polymict brec-cias, volcanogenic debris fl ow deposits, and turbidites (Clements and Hall, 2011). The breccias contain abundant volcanic clasts (basalt and andesite) as well as laminated volcaniclastic clasts, several types of limestone clasts, and a small number of dacite, granite, and metamorphic clasts. Gray-green fi ne- to medium-grained volcaniclastic turbidite sandstones are intercalated with the breccias and become increasingly abundant up section (Cle-ments et al., 2009). Many features, such as the variable and highly angular nature of breccia clasts, and contemporaneous basaltic volcanics (see discussion in Clements et al., 2009), of the Ciletuh Formation indicate active faulting in deep water, and these deposits are interpreted to represent deformation and exten-sion in a deep-marine forearc setting.
The Ciemas Formation comprises quartz-rich sandstones, pebbly sandstones, and conglomerates (Clements and Hall, 2011) (Fig. 2 and Table 1). Pebbles are predominantly vein and/or metamorphic quartz and are usually highly rounded; they are interpreted to represent the multiple recycling of sedimen-tary rocks of pre-Cenozoic age. Sandstones are typically textur-ally immature (indicated by poor sorting and angular grains) but compositionally mature (composed predominantly of quartz with a metamorphic origin). Many features indicate rapid deposition, and the formation is interpreted to have been deposited in rela-
tively shallow water on, or just off, the shelf edge (Clements and Hall, 2007; Clements, 2008).
Summary of Middle Eocene Formations
The Ciletuh and Ciemas Formations were deposited con-temporaneously in the middle Eocene and are now exposed close to each other. The two formations are texturally and composition-ally very different and are interpreted to have been deposited far from each other and juxtaposed by Miocene thrusting (Clements et al., 2009).
Upper Eocene
The upper Eocene (van Bemmelen, 1949; P. Lunt, 2006, personal commun.; R.J. Morley, 2006, personal commun.) Bayah Formation comprises dark marine mudstones and siltstones in the lower part that grade upward into quartz-rich sandstones, pebbly sandstones, and conglomerates with interbedded coals and rare limestone stringers (Fig. 2 and Table 1). Pebbly mate-rial is predominantly vein and/or metamorphic quartz and is usu-ally highly rounded and interpreted to represent the reworking of pre-Cenozoic sedimentary rocks (Clements and Hall, 2007). Paleocurrent indicators (Clements and Hall, 2011) indicate that material was sourced from the north, and the formation is inter-preted to have been deposited predominantly by large braided rivers (Kusumahbrata, 1994; Clements and Hall, 2007) as chan-nel and overbank, deltaic, and coastal plain deposits.
Lower Oligocene
The lower Oligocene Cikalong Formation (P. Lunt, 2006, personal commun.; Clements, 2008) comprises quartz-rich sand-stones, pebbly sandstones, and conglomerates intercalated with thick sequences of marine carbonaceous siltstones. These are interpreted as turbidites (Clements and Hall, 2007). Rare volca-niclastic (tuffaceous) sandstone beds indicate a contribution from a distal volcanic source.
The Oligocene Cijengkol Formation (Clements, 2008) is exposed in the Bayah Dome (Fig. 1) and comprises quartz-rich sandstones and conglomerates, volcaniclastic sandstones and con-glomerates, and shallow water coralline and foraminiferal lime-stones. Quartz-rich sandstones and conglomerates were deposited in terrestrial to shallow-marine conditions, and paleocurrent indi-cators suggest that material was sourced from the north.
METHODS
Heavy minerals were separated from 63–250 μm grain-size fraction using sodium polytungstate (SPT) solution (den-sity 2.89 g/cm3) and the funnel separation technique described by Mange and Maurer (1992). For U-Pb dating and Hf-isotope analyses, zircons were separated using a Franz magnetic separa-tor (>1.7 µA and 20° tilt angle) and diiodomethane (DIM) liquid
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with a density of 3.3 g/cm3, mounted in araldite resin on glass slides and polished. Polished zircon mounts were imaged using a refl ected light microscope in order to map positions of mounted zircon grains. Zircon U-Pb LA-ICP-MS (laser-ablation induc-tively coupled plasma mass spectrometry) dating was performed at University College London with a New Wave 213 aperture imaged frequency quintupled laser ablation system coupled to an Agilent 7500 quadrupole-based ICP-MS. External zircon stan-dard Plesovice (TIMS [thermal ionization mass spectrometry]
reference age 337.13 ± 0.37 Ma; Sláma et al., 2008) and the U.S. National Institute of Standards and Technology (NIST) silicate glass 612 (Pearce et al., 1997) were used to correct for instrumen-tal mass bias. The analytical procedure for zircon U-Pb dating is described in Stevens et al. (2010). Whenever possible, at least 60 grains per sample were analyzed in each sample (Dodson et al., 1988; Andersen 2005). Data were processed using GLITTER (Griffi n et al., 2008) and Isoplot (Ludwig, 2003, 2008) soft-ware. U-Pb ages were fi ltered using standard discordance tests
Figure 2. Simplifi ed stratigraphic column of the sedimentary sequences discussed in this chapter. Regions are shown in Figure 1.
?
?
?
MISSINGSECTION
BASEMENT
CIEMASCILETUH
CIJENGKOL.
UPPER
MID
28
29
30
31
32
33
34
35
36
37
38
39
40
41
42
43
44
45
Mid
dle
Eo
cen
eU
pp
er
Eo
cen
eL
ow
er
Olig
ocen
e
BAYAH
CIKALONG
Age(Ma) Ciletuh Bay Bayah Dome Sukabumi Padalarang
Forearc Continent
CALCAREOUS
Limestone
Turbidites
VOLCANICLASTIC
Conglomerates/breccia
OTHER
Uncertain/poorly constrained contact
Unconformity
Thrust fault
SILICICLASTIC
Quartz-richsandstoneQuartzoseconglomerate
Siltstone
KEY
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 43
with a 10% cutoff; discordant data that cross concordia within error are also included into probability-density histograms. The 206Pb/238U ratio was used to calculate ages younger than 1000 Ma, and the 207Pb/206Pb ratio for older grains (e.g., Cawood and Nem-chin, 2000). Raw data tables are presented in the supplementary data section.1
Hf-isotope analyses were performed at GEMOC ARC National Key Centre at Macquarie University, Australia. Analy-ses were performed in May 2008 using a New Wave Research 213 nm laser-ablation microprobe attached to a Nu Plasma multi-collector ICP-MS. 176Hf/177Hf ratios were measured in the same zircons that were previously dated with the U-Pb technique. The analytical procedure for Hf-isotope analyses is described in detail by Griffi n et al. (2000, 2006a). Time-resolved analyses were processed using Nu Plasma software. Analyses were car-ried out at 5 Hz frequency with a beam diameter of 55 μm and energies of ~0.1 mJ per pulse. The background was measured for 60 seconds. The length of the analysis varied between 30 and 140 seconds, depending on the thickness of the grains. Repeated analyses of Mud Tank (long-term running average 176Hf/177Hf = 0.282523 ± 43) (Griffi n et al., 2007); solution analysis 0.282507 ± 6 (Woodhead and Hergt, 2005) and 91,500 (long-term running average 176Hf/177Hf = 0.282307 ± 58) (Griffi n et al., 2006b); solu-tion value 0.282302 ± 8 (Goolaerts et al., 2004) zircon standards were used to monitor data quality (Table 2).
In addition to this, nine Cretaceous zircons from sample 28A were analyzed in April 2011 on the same Nu Plasma multi-collector ICP-MS, but with 266 nm New Wave laser-ablation
microprobe. Procedures for these analyses were identical to those carried out in May 2008. However, 40 and 60 μm spot sizes were used in April 2011 instead of 55 μm, which was used previously. During this run, Mud Tank and Temora 2 (long-term running average 176Hf/177Hf = 0.282680 ± 22) (Woodhead and Hergt, 2005); solution value 0.282686 ± 4 (Woodhead and Hergt, 2005) zircon standards were used to monitor data quality (Fig. 3).
Wherever possible, ablation spots for Hf-isotope analyses were situated on top of, or immediately adjacent to, the pits from the U-Pb analysis. Time-resolved analyses were processed using Nu Plasma software. Selection of the representative parts from laser ablation paths were based on changes in monitored intensi-ties of Hf-isotope signals. One to fi ve seconds at the beginning of each analysis were discarded in order to avoid laser warm-up-induced effects. In most instances, the laser ablation pit penetrated the whole thickness of the analyzed zircon grain. Therefore, 1 to 10 seconds at the end of each analysis were discarded in order to avoid possible contamination from the ablated glass slide. Signal intensities were used as a proxy for determinations of presence of zoning in analyzed zircon grains. No signifi cant differences were observed in signal intensities for the remainder of the laser abla-tion path, suggesting that analyzed zircons were homogeneous. These homogeneous parts of the laser ablation path were used to calculate average measured 176Hf/177Hf ratios of the analyzed zircon grain.
Interferences of 176Lu and 176Yb on 176Hf were corrected using measured intensities of interference-free 175Lu and 172Yb (e.g., Griffi n et al., 2000, 2002, 2004; Belousova et al., 2009). Analyses with 176Yb/177Hf > 0.2 or 176Lu/177Hf > 0.005 were rejected (e.g., Belousova et al., 2010).
Zircon 176Hf/177Hf ratios were used for calculating model ages. Zircon Hf model ages show time when isotopic composi-tion of zircon was identical to that of the zircon’s parental magma,
TABLE 1. COORDINATES (WGS-84) AND DESCRIPTIONS OF SAMPLES DISCUSSED IN THIS STUDY
Sample Formation Age ID Lithological description and depositional setting Lat Long
2C Bayah U. Eocene JBC2WAL137 Medium- to coarse-grained quartz-rich sandstone and conglomerate—fluvial channel sand
6.9033 106.7971
4B Bayah U. Eocene JBC2BAY187 Fine- to medium-grained quartz-rich sandstone —upper delta slope sandstone
6.9545 106.2401
8A Ciemas M. Eocene JBC2CIE259 Medium- to coarse-grained quartz-rich sandstone —shallow-marine tidal sandstone deposited on
1GSA Data Repository Item 2012130—Tables DR1–DR8: Zircon Hf and U-Pb data—is available at www.geosociety.org/pubs/ft2012.htm, or on request from [email protected] or Documents Secretary, GSA, P.O. Box 9140, Boul-der, CO 80301-9140, USA.
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which is considered to be the time when new continental crust was generated (e.g., Arndt and Goldstein, 1987; Griffi n et al., 2002; Hawkesworth et al., 2010; Belousova et al., 2010; Dhuime et al., 2011). There are three main approaches for calculating Hf model ages: (1) T
DM is calculated based on measured 176Hf/177Hf
zircon ratios and present day chondritic (CHUR) and depleted mantle (DM) values. This approach does not consider the crys-tallization (U-Pb) age of zircon, and because of this yields only a minimum estimate for the age for the source material of the zircon’s parental magma. (2) T
DMC assumes that zircon paren-
tal magma was produced from an average continental crust that originally separated from the depleted mantle (Belousova et al., 2006). T
DMC provides a more realistic estimate of source age of
analyzed zircons, because detrital zircons are mostly derived from crustal rocks. (3) T
NC assumes that most continental crust
is generated along the destructive plate margins and argues that composition of the new continental crust is isotopically enriched relative to the depleted mantle (e.g., Dhuime et al., 2011). There-fore, T
NC is calculated using isotopic signatures of island arcs that
are argued to be more representative of the newly generated con-tinental crust (e.g., Dhuime et al., 2011). Differences between model ages that are calculated using different approaches may exceed 300 m.y. (e.g., Dhuime et al., 2011).
Model ages also do not always correspond to “real” conti-nental crust formation events (e.g., Arndt and Goldstein, 1987; Kemp et al., 2006). Zircons preserve Hf-isotope signatures from all signifi cant sources that contributed to parental melts of these minerals. Model ages of zircons that are produced from mixed sources (e.g., melting of heterogeneous basement or mixed crust and mantle-derived source) will only show a geologically mean-ingless average age of all sources from which these zircons were produced. Therefore, zircon Hf model ages can be used with con-fi dence for determining ages of crust formation when only sup-ported by other lines of evidence—e.g., matching U-Pb zircon age populations.
In the present study, crustal model age data are treated as semiquantitative owing to uncertainties in calculating and inter-preting these ages. In order to avoid over-interpretation, crustal model ages are reported in Ga, and analytical errors are not given.
In order to produce a data set that is comparable to previously published Hf-isotope studies in Australia (e.g., Griffi n et al., 2002, 2004, 2006a; Belousova et al., 2009, 2010) and in Sunda-land (e.g., Sevastjanova et al., 2011), we have used an approach identical to these studies. Initial Hf-isotope ratios (176Hf/177Hf
i)
were calculated for each zircon using the 176Lu decay constant (1.865 × 10−11) (Scherer et al., 2001), measured 176Hf/177Hf ratios, and LA-ICP-MS U-Pb ages determined from the same zircon grain. The λ 176Lu decay constant (1.865 × 10−11) of Scherer et al. (2001) was used because it gives the best fi t for terrestrial rocks (Amelin and Davis, 2005; Albarède et al., 2006). The chon-dritic (CHUR) ratios of 176Hf/177Hf = 0.0332 and 176Lu/177Hf = 0.282772 (Blichert-Toft and Albarède, 1997), depleted mantle (DM) ratios of 176Hf/177Hf = 0.283251 (Nowell et al., 1998), and 176Lu/177Hf = 0.0384 (Griffi n et al., 2000), and average crustal ratio of 176Lu/177Hf = 0.015 (Griffi n et al., 2002) were used to cal-culate initial epsilon Hf (εHf
i), Hf model ages (T
DM), and crustal
model ages (TDM
C). We also use εHfi that describes the devia-
tion of zircon 176Hf/177Hf from the chondritic-meteorites evolu-tion line (CHUR) at the time of crystallization (Belousova et al., 2006; Faure and Mensing, 2004). High zircon 176Hf/177Hf
i (εHf
i
>>0) indicates mantle-derived input, and low 176Hf/177Hfi (εHf
i
<0) suggests crustal reworking (Belousova et al., 2006).
RESULTS
In this section we present results of 594 U-Pb analyses of zircon from the fi ve formations shown in Figure 2; 320 of these grains were analyzed for Hf-isotope compositions. Results are summarized in Table 3. Two samples are from the middle Eocene volcaniclastic Ciletuh Formation, which was deposited
Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 45
in a forearc setting. All other samples are quartz-rich sandstones deposited in terrestrial and marginal-marine settings. Detrital zir-con age populations range from 3629 Ma to 31 Ma in the sample set. In this study we defi ne nine populations on the basis of age “clusters” on probability-age distributions from all samples ana-lyzed (Figs. 4 and 5). Initial 176Hf/177Hf (176Hf/177Hf
i) range from
0.280847 to 0.283210, giving εHfi values from −40.0 to +18.5
and crustal model ages (TDM
C) from 0.1 to 4.0 Ga. The oldest zircon analyzed for Hf-isotope composition has a U-Pb age of ca 2.7 Ga, εHf
i −6.0, and T
DMC 3.6 Ga.
Neoarchean to Paleoproterozoic
One small population spans from Archean to Paleoprotero-zoic. Population A has an age range of ca. 2590–1717 Ma (32 grains; 7.5% of the sample set). Population A forms no distinct clusters and represents a broadly dispersed age group; 11 grains from Population A are from the Ciemas Formation. Most of the formations have very few of these grains. εHf
i values in popula-
tion A range from −18.6 to +7.6, and TDM
C values vary from 2.4 to 4.0 Ga. Most zircons in population A plot close to CHUR (11 of 28 analyzed zircons have εHf
i values between −1.8 and +1.5,
and TDM
C values of 2.4–3.0 Ga) (Fig. 6).
Mesoproterozoic to Early Neoproterozoic
Population B has an age range of 1290–723 Ma (76 grains; 15.1% of the sample set) and is represented in all samples (Fig. 4). Population B zircons have a wide range of εHf
i values
from −29.5 to +18.5, and TDM
C of 0.5–3.6 Ga.
Mid-Neoproterozoic to Cambrian
Population C has an age range of 653–480 Ma (56 grains; 13.2% of the sample set). It forms one prominent age cluster and is represented in all samples. Most of the zircons have ages between 607 and 480 Ma (49 grains; 11.6% of the sample set). Hf isotope data suggest two sub-populations. C1 is common in the upper Eocene–lower Oligocene samples and has “crustal” εHf
i
values (−28.9 to –3.6), and TDM
C of 1.7–3.3 Ga. One zircon gives an extremely low εHf
i value of ca. −40.0, and T
DMC of 4.0 Ga. C2
is common in the middle Eocene samples and has a wide range of εHf
i values from –27.0 to +5.6, and T
DMC values of 1.2–3.2 Ga.
Carboniferous and Devonian
Population D has an age range of 422–305 Ma (17 grains; 4% of the sample set) and is represented in all samples. Most of the zircons have ages between 379 and 305 Ma (15 grains; 3.5% of the sample set). Grains of this population are rare in sev-eral samples. Hf-isotope signatures reveal three sub-populations. D1 zircons (2 of 12 zircons analyzed from this population) yield “crustal” εHf
i values (−10.2 to –9.8) and T
DMC = ca 2.0 Ga. D2,
the most abundant sub-population (n = 7), yields εHfi values
Figure 3. Weighted-average plots (Ludwig, 2008) for 176Hf/177Hf val-ues in each of Mud Tank, 91500, and Temora 2 zircon standards analyses. MSWD—mean square of weighted deviates.
0.28245
0.28247
0.28249
0.28251
0.28253
0.28255
0.28257
0.28259
0.28261
Mean = 0.2825251±0.0000043 [0.0015%] 95% conf.
Wtd by data-pt errs only, 0 of 56 rej.
MSWD = 4.0, probability = 0.000
Box heights are 2 sigma
0.28228
0.28230
0.28232
0.28234
0.28236
0.28238
Mean = 0.282335±0.000027 [0.0095%] 95% conf.
Wtd by data-pt errs only, 0 of 4 rej.
MSWD = 1.8, probability = 0.14
0.28265
0.28266
0.28267
0.28268
0.28269
0.28270
0.28271
0.28272
Mean = 0.282688±0.000010 [0.0036%] 95% conf.
Wtd by data-pt errs only, 0 of 3 rej.
MSWD = 1.19, probability = 0.30
Box heights are 2 sigma
Box heights are 2 sigma
Mud Tank
91500
Temora 2
77
16
71
/fH
fH
77
16
71
fH
/fH
77
16
71
fH
/fH
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+ ++ +++− Not present Present Small cluster Prominent cluster
++
εHf T , GaDMC
–18.6 to +7.6(–1.8 to +1.5)
2.4 to 4.0(2.4 to 3.0)
–29.5 to +18.5 0.5 to 3.6
–40.0 to –3.6(–28.9 to –3.6) 1.7 to 3.3
–10.
2to
–9.8
2 .0
–2.7
to+
2 .6
1.2–
1.6
0.5–
1.0
+5
to+
12.6
–10.2 to +10.0 0.7–2.0
–12.3to –6.1
–4.9to +12.61.6–2.0 0.5–1.6
–3.9 to +15.1(+7.8 to +15.1) 0.2–1.4
–21.7 to +15.3(–1.1 to +15.3)
0.2–1.6(0.2–1.2)
–8.2 to +2.7
+11.8 to +13.8
1.0–1.7
0.3–0.5
–4.6 to +16.6 0.1–1.4
− −
9
Note: Numbers in parentheses show intervals that include the majority of zircon grains within the given population. *Three zircons have distinctly different U-Pb ages (257–263 Ma) and εHf (−14.6, −13.8, and +16.5). TDM
C (crustal model age) = 2.2 Ga and 0.2 Ga.
TABLE 3. DETRITAL ZIRCON U-Pb AGE POPULATIONS AND THEIR εHF AND TDMC IN ANALYZED SAMPLES
Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 47 47
Figure 4. Probability density plots for de-trital zircon ages presented in this study. Plots are an accumulation of individual Gaussian curves of each age measure-ment normalized to one, and measure-ment densities. Vertical bands represent age ranges for different sources; shades of gray enhance clarity. P-K—Paleocene–Cretaceous, P-T—Permian–Triassic.
(FOREARC) CILETUH FM.SAMPLE 30A
(N = 35)
Age (Ma)
Nu
mb
er
0 500 1000 1500 2000 2500 3000
(FOREARC) CILETUH FM.SAMPLE 28A
(N = 63)
CIEMAS FM.SAMPLE 8A
(N = 65)
BAYAH FM.SAMPLE 4B
(N = 60)
BAYAH FM.SAMPLE 2C
(N = 73)
CIKALONG FM.SAMPLE 22D
(N = 70)
CIJENGKOL FM.SAMPLE 13B
(N = 57)
SUNDALAND SOURCEP-K P-T
(AGES SHOWN IN FIG. 5)
ABI G F E D C
H
15
10
5
Re
lati
ve
Pro
ba
bil
ity
15
10
5
15
10
5
15
10
5
15
10
5
15
10
5
15
10
5
ARCHEANPALEO-
PROTEROZOICMESO-
PROTEROZOICNEO-
PROTEROZOICPHANEROZOIC
Mid
dle
Eo
cen
eU
pp
er
Eo
cen
eL
ow
er
Olig
ocen
e
ZIRCON POPULATIONS
Vo
lca
nic
Qu
art
z-r
ich
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 49
(–2.7 to +2.6) that are close to CHUR, and TDM
C = 1.2–1.6 Ga. D3 (n = 3) gives more “mantle-derived” εHf
i values of ca. +5.0 to
+12.6, and TDM
C = 0.5–1.0 Ga.
Permian to Triassic
Population E has an age range of 298–202 Ma (73 grains; 17.3% of the sample set). It contains two prominent sub-clusters, one between 298 and 252 Ma (23 grains; 5.4% of the sample set) and one between 246 and 202 Ma (50 grains; 11.8% of the sample set). Population E is represented in all samples, although there are notably fewer zircons from this population in the middle Eocene Ciletuh Formation samples.
Hf-isotope data show that population E can be split into three sub-populations that are similar to those identifi ed in the Malay Peninsula (Sevastjanova et al., 2011). Sub-cluster E1 has a wide range of εHf
i values (–11.4 to +10.0), and T
DMC values
(0.7–2.0 Ga). Sub-cluster E2A includes “crustal” zircons with εHf
i = –12.3 to –6.1, and T
DMC = 1.6–2.0 Ga. In the Malay Pen-
insula, this group is typical of Triassic zircons sourced from the Main Range Province. Sub-cluster E2A is most common in the lower Oligocene Cijengkol Formation. Sub-cluster E2B typically has higher εHf
i values (−4.9 to +12.6, and T
DMC 0.5–1.6 Ga). In
the Malay Peninsula, this group is typical of material derived from the Eastern Province.
Three zircons from population E (one from the Cikalong and two from the Ciemas Formations) have distinctively different U-Pb ages ca. 257–263 Ma and Hf-isotope signatures than those typical of the Malay Peninsula, suggesting that they were derived from a Permian–Triassic source other than the Tin Belt. These zircons yield very low crustal εHf
i values (−14.6 and −13.8) or
very high εHfi values (+16.5), close to those of depleted mantle.
TDM
C values are 2.2 Ga and 0.2 Ga, respectively.
Jurassic
Population F has an age range of 199–145 Ma (20 grains; 4.7% of the sample set). It forms one small, broadly dispersed age group, and is represented in all upper Eocene and lower Oligocene samples, but it is most abundant in the lower Oligo-cene Cijengkol Formation. Two grains from this population are also present in the Ciletuh Formation (Sample 30A). εHf
i values
range from −3.9 to +15.1, and TDM
C values from 0.2 to 1.4 Ga. Most population F zircons (nine of 14 zircons analyzed) have εHf
i values +7.8 to +15.1, suggesting a mantle source.
Early to Mid–Late Cretaceous
Population G has an age range of 145–74 Ma (70 grains; 16.5% of the sample set). It forms one prominent age group that is represented in all upper Eocene and lower Oligocene samples. It is present only in quartzose siliciclastic formations and is distinguished from Population H on the basis of fi eld relations (discussed below). Population G is not present in the
middle Eocene Ciemas Formation. Most population G zircons (30 of 32 analyzed) have chondritic to mantle-like εHf
i (−1.1 to
+15.3), and TDM
C = 0.2–1.2. Only two zircons yield “crustal” εHfi
of −21.7 and −12.5. These zircons have TDM
C of 1.6 and 1.3 Ga, respectively.
Latest Cretaceous to Paleocene
Population H has an age range of 110–50 Ma (37 grains; 9% of the sample set). It contains two prominent sub-clusters, H1 between 110 and 87 Ma (15 grains; 3.5% of the sample set) and H2 between 82 and 50 Ma (22 grains; 5.2% of the sample set). Population H is represented only in middle Eocene volca-nogenic forearc sandstones of the Ciletuh Formation. The two sub-clusters of population H have very different Hf-isotope val-ues. H1 has “crustal” to chondritic εHf
i values (−8.2 to +2.7), and
TDM
C = 1.0–1.7 Ga. H2 has εHfi values (+11.8 to +13.8), plotting
close to the depleted-mantle evolution, and TDM
C = 0.3–0.4 Ga.
Eocene to Oligocene
Population I has an age range of 40–31 Ma (9 grains; 2.1% of the sample set). Detrital zircon grains from Population I are present in samples 30A (middle Eocene Ciletuh Formation), 4B (upper Eocene Bayah Formation), and 22D (lower Oligocene Cikalong Formation). These grains are all of similar age to the depositional ages of the formations and were probably sourced from the Paleogene volcanic arc. Population I includes zircons with a wide range of εHf
i values (−4.6 to +16.6), and T
DMC =
0.1–1.4 Ga.
DISCUSSION
All Sundaland basement blocks are interpreted to have been rifted from the Eastern Gondwana margin (e.g., Metcalfe, 1996, 2009), and thus similarities are expected for major Precambrian zircon ages that represent regional tectono-magmatic events characteristic of Gondwana. For example, the 607–480 Ma signal present in SE Asia samples is also observed, to vary-ing degrees, in igneous and detrital rocks from South America, Africa, Antarctica, Australia, East Asia, and Europe, and is com-monly interpreted to represent processes related to the amalga-mation of Gondwana (e.g., Cawood and Buchan, 2007; Condie et al., 2009). For younger zircons, however, the different Pha-nerozoic histories of Sundaland basement terranes are likely to have produced provenance indicators specifi c to certain areas. Previous provenance studies in SE Asia (e.g., van Hattum, 2005; van Hattum et al., 2006; Clements, 2008; Hall et al., 2008) iden-tifi ed two important Sundaland source areas for Cenozoic sedi-ments, the SE Asian Tin Belt and the Schwaner Mountains of SW Borneo.
Geochronological data presented here suggest a complex provenance with several source terranes of different ages that con-tributed sedimentary detritus to West Java during the Paleogene.
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 51
A northerly derivation (from Sundaland) for all quartz-rich sand-stones is supported by detrital modes, heavy mineral assemblages, and paleocurrent data (Clements and Hall, 2011). In contrast, the Ciletuh Formation is primarily volcanogenic and was deposited in a deep-marine forearc setting (Clements et al., 2009). Based on these observations and the detrital zircon U-Pb age and Hf-isotope data (discussed below), we suggest that the Ciletuh For-mation contains detritus from temporally and spatially discrete Cretaceous and early Paleogene local volcanic arcs (situated in the area of present-day Java and West Sulawesi, respectively), whereas all other formations contain siliciclastic material derived from Sundaland.
The Middle Eocene Ciletuh and Ciemas Formations were deposited contemporaneously, although in disparate regions, and are juxtaposed in the Ciletuh Bay area (Fig. 1). Three samples from this area have been analyzed. Sample 8A is from the Ciemas Formation and contains only two Cretaceous zircons; this sample is discussed in the following section.
The two samples from the Ciletuh Formation are dominated by mid–Late Cretaceous and early Paleogene grains (Figs. 5 and 7). We observe a clear distinction between a mid–Late Creta-ceous cluster and a latest Cretaceous–Paleogene cluster (Fig. 5), particularly when comparing εHf
i values (Fig. 7). Analyzed mid–
Late Cretaceous zircons (100–80 Ma) have εHfi values that are
close to CHUR, and latest Cretaceous–Paleogene (80–50 Ma) zircons have much higher εHf
i values, plotting close to depleted
mantle (Fig. 7). We interpret the events represented by these two discrete clusters as local and having resulted from subduction-related volcanism. These volcanic rocks were then eroded and redeposited during the middle Eocene.
There is no evidence for subduction beneath the Sundaland margin between the Late Cretaceous and middle Eocene (e.g., Hall, 2009b), and this has led to the suggestion that the margin was inactive (e.g., Hall, 2009b). The termination of subduction was likely due to microcontinent collision at the Sundaland margin, which now lies beneath parts of East Java and West Sulawesi (e.g., Hall et al., 2009; Granath et al., 2011). We inter-pret the mid–Late Cretaceous ages from sample 28A to repre-sent detritus from a mature calc-alkaline arc that existed prior to early Late Cretaceous collision. The latest Cretaceous and Paleogene ages from both Ciletuh samples (28A and 30A) most likely represent a contribution from volcanic rocks exposed in West Sulawesi and Sumba that have a calc-alkaline character (e.g., van Leeuwen, 1981) and are interpreted by Elburg et al. (2002) as subduction related. West Sulawesi and Sumba were part of the E Java–W Sulawesi block (Fig. 8) and therefore already had amalgamated to Sundaland by the time subduc-tion recommenced outboard of this block (Fig. 8). We interpret the time gap between these two volcanic periods (1–2 m.y.) to mark the age of collision (ca. 80 Ma), acknowledging that it
was probably diachronous along the length of the Cretaceous Sunda margin. Crustal Hf-isotope signatures (εHf
i −8.2 to +2.7)
for the mid–Late Cretaceous zircons (population H1) support the interpretation that the arc, prior to collision, was built on old Sundaland continental crust at an “Andean-type” margin. The high εHf
i values (+11.8 to +13.8) for latest Cretaceous–
Paleogene zircons (population H2) indicate derivation from a mantle source (e.g., Belousova et al., 2006) and are comparable to those reported for the modern volcanic rocks of the Sunda Arc (Woodhead et al., 2001).
Older sources contributed to both Ciletuh samples. Sample 28A has Permian and Triassic, late Neoproterozoic, and late Mesoproterozoic age clusters. Sample 30A contains Permian and Triassic, Early Carboniferous, and Late Devonian zircons. Both samples have Proterozoic zircons. Permian–Triassic and late Pro-terozoic U-Pb zircon ages also characterize most non-volcanic siliciclastic samples (Figs. 4 and 5). These ages are interpreted to typify a Sundaland basement signature, and it is suggested that despite being dominated by a local volcanic arc compo-nent, minor contributions from Sundaland are recognizable in both middle Eocene Ciletuh samples. This is consistent with the position of the arc at the Sundaland margin, perhaps dissected by drainage systems that transported Sundaland-derived detri-tus into the forearc. However, the formation was dominated by the deposition of volcanogenic material in relatively deep water (Hall et al., 2007; Clements et al., 2009).
Sundaland Source
Middle Eocene Sedimentary RocksZircon ages from the middle Eocene Ciemas Formation are
notably different from those of the Ciletuh Formation. Only one Paleogene and two Cretaceous zircons are present. This suggests that neither the pre-collisional (mid–Late Cretaceous) Java arc nor the W Sulawesi–Sumba (latest Cretaceous–Paleogene) arc, nor any Cretaceous Sundaland sources contributed material to onshore West Java during the middle Eocene. This is consistent with the interpretation of Clements et al. (2009) that the Ciemas and Ciletuh Formations were deposited in very different set-tings and that their present proximity is not depositional but is due to thrusting. The absence of Cretaceous and Paleogene ages from the Ciemas Formation (marginal-marine quartz-rich sand-stone) supports our interpretation that Late Cretaceous and early Paleogene zircons in middle Eocene Ciletuh Formation samples (deposited to the south of Java in deep water) were not derived from Sundaland and are instead erosional products of “local” volcanic arcs.
The most prominent age clusters in the middle Eocene Ciemas Formation are Permian–Triassic and late Neoprotero-zoic (Fig. 4). These age clusters are present in all other samples described in this chapter, and their likely sources are discussed below. The Ciemas Formation contains signifi cantly more Pre-cambrian grains (46 grains [71% of sample]) than any other interval (Fig. 4). These analyses form no distinct clusters and
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are diffi cult to interpret; nevertheless they indicate a source or number of sources with various ages that were supplying detri-tus to West Java during the middle Eocene. Some of the Ciemas Formation zircon ages are not represented in other samples, sug-gesting contribution from other source rocks. Such a wide spread of ages may indicate that some of the Ciemas Formation detritus refl ects several episodes of recycling.
Upper Eocene and Lower Oligocene Sedimentary RocksUpper Eocene samples (Bayah Formation) and lower Oli-
gocene samples (Cikalong and Cijengkol Formations) have similar zircon age spectra. The most prominent age clusters are mid-Cretaceous in samples 4B, 2C, and 22D, and Late Jurassic and Cretaceous in sample 13B. Cretaceous zircon ages (popula-tion G) correspond well with known ages of Cretaceous granites
Figure 7. Plots of U-Pb ages vs. εHfi ratios for 0–300 Ma zircons from the middle Eocene, late Eocene, and early
Oligocene siliciclastic formations of West Java. Solid vertical line on the middle Eocene plot indicates our esti-mated timing of collision of East Java and West Sulawesi. VA—volcanic arc; PCV—postcollisional volcanics; DM—depleted mantle.
Cijengkol FM.
13B
22D
Cikalong FM.
Bayah FM.
2C
4B
28A
30A
8ACiemas FM.
Ciletuh FM.
n=29
n=20
n=15
n=27
n=8
n=16
n=14
en
eco
gilO r
ew
oL
en
eco
E re
pp
Ue
nec
oE
eld
diMε
fH
i
-45
-30
-15
0
15
-45
-30
-15
0
15
-45
-30
-15
0
15
TIN GRANITESVA PCV SCHWANERCRET ARC?
H
EFGI ZIRCON POPULATIONS
PERMIANCRETACEOUS JURASSICCENOZOIC TRIASSIC
Age (Ma)
0 50 100 150 200 250 300
Micro-continental
collision
DM
DM
DM
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 53
distributed across the Sunda Shelf (Williams et al., 1988) and in the Schwaner Mountains of SW Borneo (van Hattum et al., 2006). These zircon ages (population G) are older (145–74 Ma) than the Late Cretaceous and early Paleogene clusters in the Ciletuh Formation samples (population H1) that are interpreted as volcanic in origin and have distinctively different εHf
i ratios.
Predominantly high mantle-type εHfi (–1.1 to +15.3) for popula-
tion G are consistent with derivation from I-type granitoids, such as those that are common in the Schwaner Mountains (Williams et al., 1988).
Permian–Triassic, late Neoproterozoic, and latest Mesopro-terozoic to earliest Neoproterozoic age clusters are also common to the Bayah, Cikalong, and Cijengkol Formations. Permian–Triassic ages for the Bayah, Cikalong, and Cijengkol Formations,
and the middle Eocene Ciemas Formation, correspond well with known isotopic ages of Permian and Triassic granitoids distrib-uted throughout the Malay Peninsula and Indonesian Tin Islands.
Tin Belt As a Sediment SourcePermian–Triassic Tin Belt granitoids are widely exposed
throughout the Thai-Malay Peninsula and are of comparable age to Permian–Triassic zircons reported in this study. We there-fore interpret these granitoids as the main source for the W Java Permian and Triassic zircons. In the Malay Peninsula, Permian–Triassic zircons were sourced from three major magmatic suites: (1) the Permian crust–derived Eastern Province granitoids (εHf
i
from –13.3 to +9.2), (2) the Early–Middle Triassic Eastern Prov-ince granitoids with a mixed mantle- and crust-derived source
Figure 8. (A) 100 Ma plate reconstruction of southern Sundaland (modifi ed from Hall et al., 2009; Clements et al., 2011). Prior to collision of the E Java–W Sulawesi block there was subduction beneath Sundaland at the Java-Sumatra margin. WA—Woyla arc: exposed onshore Sumatra as the Woyla Group (Nappe) (e.g., Barber and Crow, 2005); IA—Incertus arc (after Hall et al., 2009), which is correlated with the Mawgyi Nappe of western Burma (Barber and Crow 2009). (B) Plate confi guration at ca. 60 Ma for southern Sundaland (base map modifi ed from Hall, 2009b; Clements et al., 2009). This shows the approximate position of the extinct Cretaceous Java-Sumatra arc after collision of the E Java–W Sulawesi micro-plate. There is subduction only beneath West Sulawesi and Sumba, and a short-lived phase of strike-slip faulting south of Java prior to the resumption of subduction beneath Sunda-land at 45 Ma.
SUNDALAND
LUCONIA Proto-South China Sea
Sabahophiolites
Lupar ophiolites
Schwanergranites
SWBORNEO
Meratusophiolites
Java
E JAVA-W
SULAW
ESI
BLOCK
W S
ulaw
esi
SumbaIndian Ocean
100°E 105°E 110°E 115°E
5°S
0°
?
E Java - W Sulawesi
10°N
0°WA
BorneoSumatra
IA
?
60 Ma
Active volcanoes
Arc prior to collision
of E Java-W
Sulawesi
A
B
100 Ma
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(εHfi values from –9.8 to +7.6), and (3) the Middle–Late Triassic
crust-derived Main Range Province granitoids (εHfi from –29.4
to –7.8, but mostly from –13.4 to –7.8) (Sevastjanova et al., 2011). We have plotted 95% confi dence ellipses for these three Permian–Triassic detrital zircon populations and have overlain these ellipses on the W Java samples (Fig. 9) to illustrate the comparisons. With few exceptions, the Eastern Province granit-oids of the Malay Peninsula appear to have been the major source of sediment for the W Java samples. Both Permian and Triassic granitoids are exposed in the Eastern Province, and zircon ages and εHf
i values from our samples broadly match those from the
Malay Peninsula. Permian and Triassic zircons from the Ciemas Formation are similar to the Malay Peninsula zircons but are on the edge of the defi ned confi dence ellipses. Two Late Permian zircons fall well outside the εHf
i confi dence ellipses from the
Malay Peninsula data set, and we suggest that these grains have a different provenance from all other Tin Belt–sourced zircons; possible alternative sources for these are discussed below. Sam-ple 13B from the lower Oligocene Cijengkol Formation contains a cluster of early Late Triassic zircons with lower εHf
i values than
those typical of the other W Java samples (Fig. 9). Most of these fall within the confi dence ellipse defi ned for Main Range Prov-ince granitoids in the Malay Peninsula, and we therefore infer that a Main Range Province source contributed signifi cantly to the Cijengkol Formation only.
Sample 13B (Cijengkol Formation) is the westernmost sample in this study, and the only sample to contain a signifi cant number of Jurassic zircons. This may indicate a (partly?) different sediment transport route and source for the formation (Fig. 10). Jurassic granitoids are reported from Central Sumatra (Cobbing, 2005), and there are very few reliable ages for Jurassic granitoids elsewhere in southern and central Sundaland. We therefore sug-gest that the presence of Jurassic zircons and εHf
i values typi-
cal of Main Range Province granitoids record a more westerly sediment transport route for the Cijengkol Formation, possibly through central and southern Sumatra, into West Java (Fig. 10).
SW Borneo As a Sediment SourceThe Schwaner Mountains (Fig. 1) are the major source
of detrital zircon in Paleogene sandstones in the region. These mountains comprise predominantly Late Cretaceous granitoids (e.g., Williams et al., 1988). Hf-isotopes have not been studied in zircons from this area. However, the Schwaner granitoids are pre-dominantly I-type, and S-type plutons are rare (Williams et al., 1988). Hence, zircons sourced from the Schwaner Mountains are expected to have positive εHf
i values. CL images (van Hattum,
2005) reveal that older zircon cores are rare. This is consistent with a predominantly mantle-like source for the Schwaner gran-itoids from this study. No fi rm evidence exists for a contribution from SW Borneo to West Java during the middle Eocene.
Sources “Outside” SundalandA similar 500–650 Ma age signal to that identifi ed in our
samples is attributed to “Pan-Gondwana” assembly and post-
collisional extension (e.g., Cawood and Buchan, 2007; Veev-ers, 2003, 2007) as well as to Ross-Delamerian orogenic cycles in eastern Antarctica and eastern Australia (e.g., Goodge et al., 2004; Glen, 2005). Similar Precambrian-age clusters are com-monly reported from detrital samples in Western Australia (Sircombe and Freeman, 1999; Cawood and Nemchin, 2000; Veevers et al., 2005, and references therein) and are often interpreted (e.g., Sircombe and Freeman, 1999) to represent provinces such as the Leeuwin block (480–850 Ma) and the Albany-Fraser orogen (1000–1300 Ma). These Proterozoic ages in W Java sandstones are therefore interpreted as recording sig-nals from basement that was once part of Gondwana but that now forms the basement to Sundaland. Paleozoic to Early Cambrian zircons have a wide range of εHf
i values. The age and spread of
176Hf/177Hfi values from these zircons closely resemble those of
zircons reported from modern rivers draining the Stanley sheet in the NE part of the Eastern Goldfi elds area of the Yilgarn Cra-ton, West Australia (Griffi n et al., 2004). Based on trace element composition, Griffi n et al. (2004) interpreted these grains as hav-ing been derived from mafi c rocks, carbonatites, and granitoid rocks. It is tempting to make correlations with sediments of the Yilgarn Craton and Western Australia, as Sundaland crust was part of Gondwana prior to breakup. However, similar-age zircons of alkaline affi nity are abundant in many Pan-Gondwana orogens (Veevers et al., 2006), indicating that these rocks, and the overly-ing sediments, probably have a complex history of erosion and redeposition.
Thick, laterally extensive sedimentary sequences of Jurassic and Early Cretaceous age exposed over large areas of Indochina and the Malay Peninsula are referred to as the Khorat Group and lateral equivalents (Racey, 2009). It is unclear how far south these and equivalent sequences extended prior to regional uplift in the Late Cretaceous and development of the SE Asia Regional Unconformity (Clements et al., 2011), but it is probable that some of these rocks were eroded and transported elsewhere in Sundaland. Other sources of pre-Cenozoic sedimentary rocks in the region include, for example, SE Java, where zircons of vary-ing ages (many are Archean and Proterozoic) have been incorpo-rated into Cenozoic volcanic rocks as xenocrysts and transported to the shallow crust by volcanic processes (Smyth et al., 2007). These volcanic rocks are clearly sampling an older source, and the large variation in ages within these rocks was interpreted by Hall et al. (2009) to indicate a sedimentary source rather than crystalline basement.
Recent discoveries of deep, pre-Cenozoic sedimentary basins, or keels, in the NE Java Sea (e.g., Granath et al., 2011) reveal huge volumes of sedimentary rocks that could have con-tributed detritus to Cenozoic sequences during episodes of uplift, for example, in the Late Cretaceous. Granath et al. (2011) used newly acquired long-offset, long-record seismic data to identify a sedimentary section up to 8.5 km thick preserved within a fault-bounded basin beneath the Cenozoic sedimentary section in the NE Java Sea; they interpreted these sequences as Mesozoic to possibly Precambrian in age. This interpretation implies that
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 55
Figure 9. A comparison of the Hf-isotope compositions of Permian–Triassic zircons from modern rivers in the Malay Peninsula (Sevast-janova et al., 2011), representing the Tin Belt source, and Paleogene sandstones in West Java. Fields are defi ned as 95% confi dence ellipses. DM—depleted mantle.
U-Pb age, Ma
JBC2191
JBC2117
JBC2187
JBC2137
JBC2259
JBC2272
JBC3145
Lower
Oligocene
Cijengkol Fm.
Lower
Oligocene
Cikalong Fm.
UpperEocene
Bayah Fm.
MiddleEocene
Ciemas Fm.
MiddleEocene
Ciletuh Fm.
The Malay
Peninsula;
Tin Belt
IS40
IS37
IS2
-45
-30
-15
0
15
εHf
200 210 220 230 240 250 260 270 280 290 300 310
-45
-30
-15
0
15
-30
-15
0
15
-45
-30
-15
0
-45
15
-45
-30
-15
0
15
-45
-30
-15
0
15
DM
DM
DM
DM
DM
DM
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these basins developed on continental crust prior to the breakup of Gondwana and therefore are fi lled with sedimentary rocks that record an early Australian–Greater Indian history before they were incorporated in SE Asia. Similar sedimentary sequences may be partly preserved in other parts of Sundaland, for example, between W Java and SW Borneo. These sequences could have been eroded during the early Paleogene and contributed polycy-clic sedimentary detritus to the Paleogene sequences discussed in this paper. For example, several differences between the Ciemas Formation (sample 8A) and all other samples discussed in this study may indicate a contribution from a different source. As pre-viously highlighted, Hf-isotope compositions of the two Permian zircons in the Ciemas Formation fall well outside the 95% con-
fi dence ellipses defi ned from the Malay Peninsula (Sevastjanova et al., 2011). These are unlikely to have been sourced from the Malay Peninsula and therefore indicate a different Permian source in the region. There are also many more Paleozoic zircons in the Ciemas Formation sample, and although these cannot be linked to any particular source, they must represent a complex history that is at least partly different from that of all other samples.
These interpretations are tentative and are based on few analyses; more data are required in order to understand the contri-bution to Paleogene SE Asia sediments from alternative Permian–Triassic and older sources. Geochronological studies similar to the one presented here, which combine U-Pb and Hf-isotope techniques, will be hugely benefi cial in helping to determine
SUMATRA
BORNEO
JAVA
Schwanerinput
PENINSULARMALAYSIA
Tin-Beltinput
SCHWANERMOUNTAIN
LATE EOCENE
SUMATRA
PENINSULARMALAYSIA
BORNEO
Volcanic arccontribution
NoSchwaner
input
JAVA
E PROVINCEGRANITOIDS
Tin-Beltinput
SCHWANERMOUNTAINGRANITES
MIDDLE EOCENE
E PROVINCEGRANITOIDS
?
?
?
??
?
?
Source area Emergent land Drainage
0°
5°S
110°E105°E
?
0°
5°S
110°E105°E
SUMATRA BORNEO
Possible waningof Schwaner?
JAVA
PENINSULARMALAYSIA
SCHWANERMOUNTAINGRANITES
Tin-Beltinput
EARLY OLIGOCENE
?
?
?
110°E105°E
0°
5°S
E PROVINCEGRANITOIDS
MAIN RANGEGRANITOIDS
Sumatrainput?
Figure 10. Schematic paleogeographic maps of the Sunda Shelf region for the middle and late Eocene, and early Oligocene. During the mid-dle Eocene there was no contribution from the Schwaner Mountains to West Java. The Ciletuh Formation was deposited in deep water to the south and was sourced mainly from local volcanic arcs with only a minor contribution from Sundaland. During the late Eocene both the Schwaner Mountains and the Tin Belt granitoids were supplying ma-terial to West Java. During the early Oligocene there was a possible waning of the Schwaner Mountains source. There was also a contri-bution from Sumatra as indicated in the early Oligocene. Paleodrain-age in the area between the Malay Peninsula and northern Borneo is from van Hattum (2005), and in southeastern Borneo from Witts et al. (2011). Gray triangles indicate areas that are being eroded and are not necessarily mountainous areas. The black dashed line represents a paleodrainage divide that was proposed by Smyth (2005) to account for the lack of Tin Belt and Schwaner sources in East Java. Java and Borneo have been rotated in accordance with tectonic reconstructions (Hall, 2002).
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Detrital zircon U-Pb age and Hf-isotope perspective on sediment provenance and tectonic models in SE Asia 57
paleosediment-routing systems and improve future tectonic mod-els, particularly in SE Asia where active tectonism, arc volca-nism, and a tropical climate have partly obscured the fi ner details of a rich and complex tectonic history.
Summary and Conclusions
U-Pb ages of detrital zircon suggest four major sediment sources for the Paleogene sandstones in West Java. These are (1) a latest Cretaceous–Paleogene volcanic arc in West Sulawesi–Sumba, (2) a Cretaceous volcanic arc in Java-Sumatra, (3) a Cre-taceous granitic suite in the Schwaner Mountains in SW Borneo, and (4) granitoids of the Thai-Malay Tin Belt. Hf-isotope data reveal source regions and histories that could not have been iden-tifi ed by U-Pb analyses alone.
Relatively few zircons were derived from the Eocene–Oligocene Sunda arc, indicating that a geographical divide existed between the arc and onshore Java at this time. This is consistent with paleogeographic interpretations (Clements and Hall, 2007) that show the arc submerged and farther south than its present position.
Two Cretaceous populations of zircons in the Ciletuh For-mation are based on U-Pb age and Hf-isotope compositions, which we interpret as representing two different volcanic arc systems. The fi rst was active in the Cretaceous and developed in Java-Sumatra as a consequence of Tethyan subduction beneath Sundaland, which ended at ca. 80 Ma. The second was active in the latest Cretaceous and Paleogene (from ca. 80 Ma) and devel-oped as a consequence of subduction beneath West Sulawesi and Sumba that probably ceased in the early Eocene. Hf-isotope compositions indicate that the Java-Sumatra arc was built on Sundaland continental crust at an “Andean-type” margin. The W Sulawesi–Sumba arc was characterized by higher εHf
i (man-
tle-like ratios) comparable to those of the present-day Sunda Arc. The break between zircon U-Pb ages (ca. 80 Ma), and therefore between these two volcanic episodes, is interpreted here as repre-senting the docking of the E Java–W Sulawesi microcontinent to Sundaland. This collision had a signifi cant impact on the region and resulted in the cessation of subduction beneath much of Sun-daland (except West Sulawesi) and was followed by a period of regional uplift and erosion (Clements et al., 2011) until subduc-tion resumed again at ca. 45 Ma.
A SW Borneo source (the Schwaner Mountains) is charac-terized by mid-Cretaceous ages and is interpreted as the main source of Cretaceous zircons other than the slightly younger volcanic ages typical of the Ciletuh Formation. Overlap in U-Pb zircon ages from SW Borneo and the Java-Sumatra volcanic arc can blur the distinction between these two sources. However, dis-tinctively different Hf-isotope signatures for these grains allow differentiation between the two Cretaceous zircon populations. Cretaceous zircons from upper Eocene and lower Oligocene for-mations are characterized by high εHf
i values that are consistent
with provenance from the I-type granitoids, such as those typi-cal of the Schwaner Mountains. Conversely, Cretaceous zircons
from the middle Eocene Ciletuh Formation have much lower εHfi
values and are interpreted here to be from a volcanic arc. The absence of mid–Late Cretaceous zircons in the Ciemas Forma-tion suggests that SW Borneo was not supplying detritus to West Java in the middle Eocene.
Granitoids of the Thai-Malay Peninsula are interpreted to be the major source of Permian and Triassic zircons in the W Java sandstones. Sevastjanova et al. (2011) determined the Hf-isotope compositions typical of the Malay Peninsula Main Range and Eastern Province granitoids, and this has been used to assess the contribution from this area. The upper Eocene Bayah Formation and lower Oligocene Cikalong Formation contain Permian and Triassic zircons that were derived from the Eastern Province. The Cijengkol Formation appears to have a mixed Eastern and Main Range Province provenance and is the only sample to contain a signifi cant Jurassic cluster. Jurassic granitoids are known from Sumatra, and therefore a paleo-drainage system through present-day central and southern Sumatra is inferred for the Cijengkol Formation.
A few Permian–Triassic zircons have εHfi values that
fall outside the 95% confi dence fi eld defi ned for a Tin Belt source, suggesting a minor contribution from an alternative Permian–Triassic source that is, at present, uncertain. Cambrian and Precambrian zircons are present in all samples and probably represent a contribution from crystalline basement as well as reworked (pre–early Mesozoic) sedimentary sources.
The results presented here illustrate the immense potential of Hf-isotope analysis of dated zircons to improve and expand the interpretation of detrital zircon studies. The Hf-isotope data provide a tool to distinguish between source rocks of similar age but different geological histories. They also give insights into the genesis of the source rocks involved, which is invaluable in the reconstruction of tectonic settings. Thus in the present study the Hf-isotope data have allowed us to identify the presence of ancient crust beneath the Java-Sumatra arc and to recognize an Andean-style margin. This is a fi nding with both tectonic and economic-geology signifi cance. The addition of such high-precision in situ Hf-isotope data to a set of dated zircons is, by comparison with the U-Pb analysis itself, both rapid and inexpensive. It should become a standard tool in future detrital zircon studies.
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