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Geochemistry and detrital geochronology of stream sediments from East
Timor: Implications for the origin of source units
Article in Australian Journal of Earth Sciences · June 2013
DOI: 10.1080/08120099.2013.810664
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Geochemistry and detrital geochronology of stream
sediments from East Timor: implications for the origin of
source units
P. A. Dinis
a
, C. Tassinari
b
& M. M. S. Cabral Pinto
c
a
IMAR-CMA Marine and Environment Research Centre, Department of Earth Sciences, Largo Marques
de Pombal , Coimbra , 3000-272 , Portugal
b
Instituto de Geociências , Universidade de São Paulo/CPGeo , Rua do Lago 562, SP CEP 05508-080,
São Paulo , Brazil
c
GeoBioTec, Department of Geosciences , University of Aveiro , Campus de Santiago, 3810-193,
Aveiro , Portugal
Published online: 26 Jun 2013.
To cite this article: P. A. Dinis , C. Tassinari & M. M. S. Cabral Pinto (2013) Geochemistry and detrital geochronology of stream
sediments from East Timor: implications for the origin of source units, Australian Journal of Earth Sciences: An International
Geoscience Journal of the Geological Society of Australia, 60:4, 509-519, DOI: 10.1080/08120099.2013.810664
To link to this article: http://dx.doi.org/10.1080/08120099.2013.810664
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3. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
Geochemistry and detrital geochronology of stream
sediments from East Timor: implications for the origin
of source units
P. A. DINIS1
*, C. TASSINARI2
AND M. M. S. CABRAL PINTO3
1
IMAR-CMA Marine and Environment Research Centre, Department of Earth Sciences, Largo Marques de
Pombal, 3000-272 Coimbra, Portugal
2
Instituto de Geoci^
encias, Universidade de S ~
ao Paulo/CPGeo, Rua do Lago 562, S ~
ao Paulo, SP CEP 05508-080,
Brazil
3
GeoBioTec, Department of Geosciences, University of Aveiro, Campus de Santiago, 3810-193 Aveiro, Portugal
Crustal fragments with Asian and Australian affinities that outcrop on the island of Timor were stacked
together owing to the collision between the Banda volcanic arc and the Australian continent. Geo-
chemistry of floodplain sediments (11 samples) and detrital zircon geochronology of bedload sediments
(5 samples) are used to interpret the geological nature of the source units exhumed in East Timor. The
geochemical data revealed source rocks with widely variable proportions of felsic and mafic material.
In general, the Banda Terrane units supply higher proportions of mafic material, which tend to have
lower zircon productivity, than the Australia Passive Margin or Gondwana sequences. Zircon with ages
of 2150–1500 and 365–210 Ma constitute the most common populations in all stream samples. Sampling
sites that are not sourced exclusively by the Gondwana Sequence and have Banda Terrane units in
their watersheds are characterised by high proportions of Triassic zircon, which are common in the Sula
Spur, and discordant grains. It is proposed that a significant component of the zircon found in the
allochthonous units of Timor is inherited from Australian-related crustal fragments that drifted from the
Sula Spur. These units were carried south as the Banda Arc progressed towards the Australian continent
and emplaced in Timor with the Banda Terrane.
KEY WORDS: East Timor, provenance, detrital zircon, SHRIMP, geochemistry, arc–continent collision
INTRODUCTION
Arc–continent collision-related regions comprise dis-
tinct fragments of upper plate that are stacked together
owing to orogenic movements and whose geology can be
evaluated from a study of coeval or succeeding sedimen-
tary deposits (Dorsey 1998; Harris et al. 2000; Gabo et al.
2009; Weber et al. 2010). The island of Timor is geneti-
cally related to an arc–continent collision as part of the
non-volcanic outer arc that, coupled with a volcanic
inner arc, defines the Banda Arc system. The Banda Arc
is located in the region of convergence of the Eurasian
plate with the northward-moving Indo-Australian plate
and the westward-moving Philippine Sea–Pacific plate
(Figure 1). Depending on their location, the islands of
the outer Banda Arc are likely to incorporate units asso-
ciated with different plate fragments.
The geological formations of Timor may be organised
into autochthonous or para-autochthonous and allo-
chthonous units (Audley-Charles 1968; Rosidi et al.
1979). These units reveal either Australian or Asian
affinities and comprise metamorphic complexes, fore-
arc ophiolites and unmetamorphosed continental shelf
sediments with markedly distinct compositions. The dis-
tribution of the different crustal fragments in Timor is
associated with thrust sheets whose geometry is still
imprecisely known. Furthermore, the exact nature of
each of the thrust slices is not agreed, particularly in
what regards the metamorphic complexes (Barber &
Audley-Charles 1976; Charlton 2002; Kaneko et al. 2007;
Standley & Harris 2009) and the ophiolite-like units
(Hamilton 1979; Berry 1981; Harris & Long 2000; Falloon
et al. 2006).
The investigation of the geology of East Timor has
been hampered by an armed conflict and the social insta-
bility that lasted from the mid 1970s until recently.
Although the country presently benefits from globally
peaceful conditions, fieldwork in the region is still diffi-
cult owing to the orographic features of the island and
the poor roads and tracks, making access to many out-
crops difficult. An indirect interpretation of the nature
of the crustal fragments accreted owing to the arc–conti-
nent collision may be achieved from the analyses of
stream sediments.
*Corresponding author: pdinis@dct.uc.pt
Ó 2013 Geological Society of Australia
Australian Journal of Earth Sciences (2013)
60, 509–519, http://dx.doi.org/10.1080/08120099.2013.810664
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4. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
We present here the geochemistry and detrital geo-
chronology results from stream sediments collected at
downstream locations of some of the largest streams of
East Timor. One sampling site is entirely sourced by
units with Australian affinity, while the remaining sites
have catchments that include variable proportions of
Asian and Australian affinity units (Table 1). The article
is focused on the geochemical signal of fine-grained
floodplain sediments and the geochronology of detrital
zircon grains from coarse-grained bedload sediments.
Sensitive high-resolution ion microprobe (SHRIMP) geo-
chronology data from Timor are presented here for the
first time. The present work aims to contribute to the
characterisation of the plate fragments exhumed in
the island of Timor and to distinguish these plate
fragments on the basis of the geochemistry and geochro-
nology criteria.
GEOLOGICAL SETTING
The outer and inner Banda are situated between Aus-
tralia (to the south), New Guinea (to the east and north)
and Sulawesi (to the west), defining a 180
curve that
extends for more than 1000 km long in its outer edge.
Timor Island is located in the southern arm of the outer
arc and is separated from the inner arc by approxi-
mately 25 km (the distance between Dili and the island
of Atauro).
The evolution of SE Asia is marked by a sequential
removal of crustal fragments from northern and western
Australia that drifted northward and eventually coa-
lesced with SE Asia (Audley-Charles 1983; Seng€
or 1987;
Metcalfe 1998; Hall 2012). Hall (2012) recently published a
comprehensive reconstruction of the evolution of the
region. Based on the timing of Gondwanaland block
Figure 1 Geological framework of the Banda Arc region and Timor Island. (a) Tectonic setting of the Banda Arc between Indo-
Australian, Pacific–Philippine and Eurasian plates. Arrows express convergence vectors between Indo-Australian (AUS), Eur-
asian (EUR), Philippine Sea (PSP) and Pacific (PP) plates as indicated in Hall (2009). BA: Banda Arc; BS: Banggai-Sula. (b) Sim-
plified geological map of Timor Island based on Audley-Charles (1968) and Rosidi et al. (1979), and subsequent modifications
presented in geological sketches of Harris (2006) and Kaneko et al. (2007). Location of sampling points is also represented.
(c) Schematic cross section from Standley Harris (2009).
510 P. A. Dinis et al.
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5. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
dispersal and SE Asia accretion, some authors differenti-
ate Sundaland, where the accreted fragments ended up
during the Mesozoic, and eastern Indonesia, where the
accretion is Cenozoic (e.g. Charlton 2001; Hall 2009). The
region between Sundaland and the Australian continent
passed through dramatic changes during the Cenozoic
that, among others, include the development of the
Banda Arc.
Numerous geological surveys in east and west Timor
demonstrate that the island is composed of plate frag-
ments with Australian and Asian affinities that were
brought together during the Neogene crustal shortening
(Audley-Charles 1968; Grady Berry 1977; Charlton et al.
1991; Harris 1991; Harris et al. 2000; Villeneuve et al. 2005;
Standley Harris 2009). Hall Sevastjanova (2012)
pointed out that, because SE Asia includes crustal blocks
detached from the Australian margin, and their collision
with SE Asia continued until the Neogene, the term
Australian affinity is vague and does not consistently
distinguish crustal fragments of contrasting geological
evolutions. For simplicity, we adopted the distinction
between Australian and Asian affinity units presented
in previous works on the geology of Timor.
The geological units with Australian affinity in Timor
are the Permian to Middle Jurassic Gondwana Sequence
and the Upper Jurassic to Miocene Australian Passive
Margin Sequence (Harris et al. 2000). These sequences
were deposited, respectively, in a syn-rift extensional
basin and in a passive margin after Late Jurassic break-
up of northern Gondwana. The Banda Terrane (Asian
affinity) consists mainly of seafloor metamorphosed
rocks and interbedded sediments. The presence of volca-
nic rocks associated with an arc setting, Cenozoic
turbidites and fossils of Asian affinities distinguish the
Banda Terrane from the continental margin of Australia
(Standley Harris 2009). Although an overall Asian
affinity has been postulated, it includes crustal
fragments of Australian origin that docked with SE Asia
at different times (Milsom et al. 2001; Standley
Harris 2009).
Most authors agree that the Indo-Australian plate has
been subducting beneath the Banda Arc, although the
timing and detailed evolution of this continent–island
arc collision are contentious. For some, the Banda Sea
formed by late Neogene expansion as a back-arc basin
during the Neogene (Honthaas et al. 1998; Hinschberger
et al. 2005). The Banda Arc developed after the collision
between the Sula Spur (an elongated portion of the Aus-
tralian continent that extended WNW from New Guinea)
and west Sulawesi (part of the Eurasian continent) dur-
ing the Miocene (Milsom et al. 2001; Hinschberger et al.
2005; Hall 2012). In other models, the Banda Arc started
to form when the Java Trench, where the Indian Ocean
has been consumed below Sundaland since the Eocene,
propagated eastwards at the contact between oceanic
crust of the Banda Embayment (between the Sula Spur
and Timor) and continental crust of SE Asia (Spakman
Hall 2010; Hall 2012). In this model, it is considered
that the islands of the inner Banda Arc moved progres-
sively towards the Australian margin (and Timor) owing
to rollback of the subduction hinge and that the overall
present geometry of the arc is a result of the curvature of
the Australian margin that surrounds it to south, east
and northeast. Audley-Charles (2004) proposed that the
collision of the Australian continental margin and
Banda Arc started at approximately 3.5 Ma. For Keep
Haig (2010), the initial collision-related deformation in
Timor began shortly after 10 Ma, with an interval of tec-
tonic quiescence from 5.5 to 4.5 Ma, followed by uplift
and extension. The intense Neogene uplift in the Banda
Arc has been demonstrated by several researchers
(Charlton et al. 1991; Milsom et al. 2001; Audley-Charles
2004; Hinschberger et al. 2005; Kaneko et al. 2007; Roos-
mawati Harris 2009; Nguyen et al. 2013) but there is lit-
tle agreement about the specific tectonic regime.
MATERIALS AND METHODS
Eleven sampling sites in downstream locations of East
Timor streams were selected for this study
. The delimita-
tion of the catchments that drain to the sampling points
and the analysis of the drainage network were per-
formed using a Digital Elevation Model (DEM) based on
a Shuttle Radar Topography Mission (SRTM) image. The
DEM data were processed with the package Arc Hydro
Table 1 Location of the sampling points and proportion of different geological units in their catchment areas.
Sampling
point
Latitude
(south)
Longitude
(east)
Australian
affinity (%)
Asian
affinity (%)
Recent
(%)
1 9.0861 125.6923 11.5 83.3 5.2
2 9.0930 125.6892 37.4 37.1 25.5
3 9.1399 125.5461 73.8 4.6 21.6
4 9.1705 125.4479 96.8 3.2
5 9.2034 125.4062 82.4 14.1 3.5
6 9.2750 125.3188 48.1 50.6 1.3
7 8.7425 125.1309 69.2 4.8 26.0
8 8.5531 125.5354 100.0
9 8.4757 126.5280 60.8 12.8 26.4
10 8.5376 126.1667 80.4 16.2 3.4
11 8.5170 125.9994 78.6 21.4
Australian affinity: Gondwana and Australian Passive Margin sequences and Aileu Complex; Asian affinity: Banda Terrane and
ophiolite-like units; Recent: Syn- to post-orogenic sediments.
Stream sediments, East Timor 511
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6. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
(ArcGIS 10). Geochemical and geochronological analyses
were conducted on fine-grained floodplain sediments
from each sampling site and five selected coarse-grained
bedload sediments, respectively. The sediment samples
were collected with shovel and hand tools during
November 2011.
The proportions of major elements in floodplain sedi-
ments were determined by X-ray fluorescence after lith-
ium borate fusion. Most trace elements were determined
by ICP mass spectrometry following a lithium borate
fusion and nitric acid digestion. Given the fine-grained
character of the sampled sediments and the expected
effectiveness of fusion when determining most elements
with ICP (Walsh 1997), element underestimation owing
to incomplete dissolution is thought to be limited. Base
metals were determined after aqua regia digestion.
These analyses were performed at the laboratories of
ACME Analytical.
Zircon grains were separated using standard techni-
ques, involving heavy liquids apparatus and a Frantz iso-
dynamic magnetic separator, in the laboratories of the
Earth Sciences Department of University of Coimbra
(Portugal). Zircon grains were later washed, mounted in
epoxy resin and polished, together with the Temora 2
standard, for cathodoluminescence imaging and U–Pb
dating, at the laboratories of University of S~
ao Paulo
(Brazil). Polished mounts were comprehensively
examined with a FEI-QUANTA 250 scanning electron
microscope equipped with secondary-electron and catho-
doluminescence. Isotopic analyses were performed on
the SHRIMP II ion microprobe following the analytical
procedures presented in Williams (1998) using a primary
oxygen ion beam in the range 6–4hA for a spot diameter
of 30 mm. Uranium abundance and U/Pb ratios were cali-
brated against the Temora 2 standard. Correction for
common Pb was made based on the basis of the 204
Pb
measured. Isoplot 3.72 (Ludwig 2003) and AgeDisplay
(Sircombe 2004) were used, respectively, for creating the
concordia diagrams and the combined probability-
histogram plots. Only data with discordance below 10%
or that cross concordia within error were included in
the probability and histogram plots.
RESULTS AND DISCUSSION
Geochemistry of floodplain sediments
The proportions of major elements and selected minor
elements are shown in the Supplementary Papers
(Appendix 1) and in bivariate and ternary diagrams
(Figures 2, 3). In this work, we present only the analyses
of minor and trace elements that tend to be immobile
and are commonly used to establish sediment
provenance.
In terms of major elements, the fine-grained flood-
plain sediments have moderate SiO2 (51.9–61.4%, average
56.0%) and Al2O3 (12.5–18.5%, average 13.7%) and rela-
tively high Fe2O3þMgO (6.2–13.1%, average 8.5%) con-
tents. The proportions of CaO, MgO, Na2O and K2O show
considerable scatter. Highest contents of Fe2O3, MgO and
Na2O are found in TR1, TR2, TR3 and TR11, which dis-
play relatively low K2O. Conversely, TR8 is distinguished
by its high K2O and low MgO and Na2O. The proportions
of TiO2, MnO, P2O5 and Cr2O3 are always lower than 1%,
with the exception of samples TR1, TR2 and TR11, which
are slightly enriched in TiO2.
The abundances of Zr (124.5–255.4 ppm), V (65–
205 ppm), Rb (42–159 ppm), Y (21.9–34.6 ppm), Ni (24.9–
40.7 ppm), Sc (11–26 ppm), Th (6.8–20.5 ppm), Co (10.7–
21.4 ppm), Nb (10.3–18.4 ppm), Hf (3.3–6.6 ppm) and U
(1.2–3.1 ppm), are highly variable. Samples TR1, TR2,
TR3 and TR11, with high Fe2O3 and MgO, also tend to
have higher Co, Ni, Sc, and V contents, while Nb, Rb, Th,
U and Zr are substantially higher in TR8 than in the
other sediments. Rb, Th and U correlates with K2O, indi-
cating that these elements are present in K-bearing min-
erals or associated with a paragenesis that contains an
important proportion of K-bearing minerals.
The proportions of rare earth elements (REE) are also
variable (total content between 111.68 and 238.33 ppm).
The pattern of REE is relatively uniform, with enrich-
ment in light REE (10.1 (La/Yb)N 4.8; ‘N’ referring to
chondritic normalisation), flat heavy REE (1.78 (Gd/
Yb)N 1.42), distinguishable Eu-anomalies (0.57 Eu/
Eu
0.75) and indistinguishable Ce-anomalies (Ce/Ce
0.93) (Figure 4a). Samples TR1, TR2, TR3 and TR11 display
a PAAS-normalised (normalised to Post-Archean Average
Australian Shale, after Nance Taylor 1976) pattern
characterised by a slight enrichment in heavy REE,
while the other sediments tend to have flatter patterns,
which are particularly evident in TR8 and TR9
(Figure 4b). Most samples show lesser light REE propor-
tions than the Upper Continental Crust (UCC; after Tay-
lor McLennan 1985), with the exception of TR8, which
is enriched in all REE, and TR4 and TR7, which display
comparable REE abundances. Sample TR8 is also charac-
terised by substantially higher REE content, (La/Yb)N
and (La/Sm)N ratios, and Eu anomaly than the other
floodplain sediments.
Discrimination diagrams based on major and minor
elements geochemistry have been used in attempts to
distinguish the tectonic setting of depositional basins.
Although the composition of sedimentary rocks depends
on numerous factors and the application of this dia-
grams has been challenged by several authors (Van de
Kamp Leake 1985; Haughton et al. 1991; Armstrong-
Altrin Verma 2005), they can give valuable informa-
tion on the nature of the source rocks and help to discern
the relative contribution of units with Australian
(derived from a continental margin) and Asian (with arc-
related rocks) origin.
Traditional diagrams point to substantially different
source units. Samples TR1 and TR11 are plotted in the
fields characteristic of ‘ocean island arcs’ (from Bhatia
1983) or ‘arc setting, basaltic and andesitic detritus’
(from Roser Korsch 1986) (Figure 2a–e). The diagrams
La–Th–Sc, Th–Co–Zr/10, Th–Sc–Zr/10 and La/Sc vs Ti/
Zr (Bhatia Crook 1986) also associate these sediments
with oceanic island arc settings (Figures 2e, 3). Samples
TR8 and TR9 fall in the fields of active continental mar-
gins on most discrimination diagrams. Samples TR2,
and TR3 are more akin to ocean island arc settings,
while samples TR4, TR5, TR6, TR7 and TR10 are in gen-
eral placed in the fields of continental island arc or
evolved arc setting. None of the studied sediments plot
in the fields of passive margins.
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7. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
Figure 2 Plots of floodplain sediments in bivariate discriminant diagrams of tectonic setting and source rock nature. (a) K2O/
Na2O vs SiO2 (Roser Korsch 1986). (b) SiO2/Al2O3 vs K2O/Na2O (Roser Korsch 1986). (c) TiO2 vs Fe2O3þMgO (Bhatia 1983).
(d) Al2O3/SiO2 vs Fe2O3þMgO (Bhatia 1983). (e) Ti/Zr vs La/Sc (Bhatia Crook 1986). (f) La/Th vs Hf (Floyd Leveridge 1987).
(g) K2O vs Rb (Floyd Leveridge 1987). (h) Co/Th vs La/Sc with average composition of igneous rocks from Condie (1993);
FVR: Felsic volcanic rocks. (i) Th/Sc vs Zr/Sc (McLennan et al. 1990). (j) Th/Co vs Zr/Co (McLennan et al. 1993). Samples
selected for SHRIMP analyses are identified.
Stream sediments, East Timor 513
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8. TAJE_A_810664.3d (TAJE) 17-07-2013 10:57
When Zr/Co and Th/Co contents are plotted together,
all samples fall on a linear trend, indicating wide dis-
tinct felsic- and mafic-rich source units and minor recy-
cling (Figure 2j). In general, the geochemical results
indicate that TR1 and TR11 contain the highest propor-
tions of material derived from mafic source rocks. The
enrichment in mafic material in these sediments may in
part be explained by the greater exposure of the Banda
Terrane in their catchments. The basic volcanic rocks of
the Maubisse Formation that outcrop to the south of the
Aileu Complex (Audley-Charles 1968; Charlton 2001) are
also likely to source significant amounts of the mafic
component to TR11. On the opposite side, sample TR8
includes more felsic material than the other sediments,
as is particularly evident from the diagram Rb vs K2O
(Figure 2g). The overall higher concentration of REE,
along with other features of the REE patterns, like the
enrichment in light REE, fractionation of light REE cou-
pled with flatter heavy REE patterns, and higher nega-
tive Eu anomaly, also suggest felsic source units
(Figure 4). All these features are compatible with the tec-
tonic setting discrimination based on the proportions of
major and minor elements, which relates its source
rocks with a continental margin.
U–Pb zircon geochronology of bedload
sediments
The majority of the zircon grains are rounded to sub-
rounded or sharp broken fragments of variable size
(Figure 5). A few euhedral prisms and pyramids are
observed. Large fragments of acicular grains are fre-
quent in sample TR6 while the other samples contain
more equant morphologies. The internal structures are
widely variable. Rimmed zircons that can have markedly
distinct to faintly visible bands of variable thickness are
the most common. A significant proportion of the sam-
pled zircons comprise xenocrystic cores enclosed by con-
centric zircon rims (Figure 5). Some grains are
apparently unzoned while others display patchy or oscil-
latory zoning. A significant number of grains reveal
micro-fractures.
The analytical results are presented in the Supple-
mentary Papers (Appendix 2). Most zircons show Th/U
ratio higher than 0.2. In total 147 age analyses were per-
formed, although numerous measurements (50) did not
give concordant (90–100%) results. The proportion of dis-
cordant ages is lower in TR8 (18%) than in the other sam-
ples (30–54%). The zircon ages span a wide age range
Figure 3 Plots of floodplain sediments in ternary discrimi-
nant diagrams of tectonic setting (Bhatia Crook 1986).
Samples selected for SHRIMP analyses are identified.
Figure 4 REE patterns of the floodplain sediments. (a) Sam-
ple concentrations normalised to chondrite. (b) Sample con-
centrations normalised to PAAS.
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9. TAJE_A_810664.3d (TAJE) 17-07-2013 10:58
(Figures 6, 7) with the most common populations at:
Paleoproterozoic to early Mesoproterozoic (ca 2150–1500
Ma), late Mesoproterozoic to early Neoproterozoic (ca
1300–900 Ma), Ediacaran to middle Ordovician (ca 630–
460 Ma) and latest Devonian to Triassic (ca 365–210 Ma)
(Figure 6). Beside these major groups, a few analyses
gave ages older than 2300 Ma (early Paleoproterozoic and
Archean; oldest zircon of ca 3.4 Ga) and of approximately
750 Ma and 400 Ma.
Several sampled grains display cores and rims of sub-
stantially different ages (Figure 5). The older Archean to
Mesoproterozoic results were usually obtained in cores
mantled by younger zircon. Paleozoic and Neoprotero-
zoic ages were obtained from both cores and rims.
Mesozoic ages were found to be more common in outer
rims, but were also obtained from the centre of fine-
grained zircon.
A total of 57 age determinations from sample TR8
gave 47 concordant results that span between 2875 and
254 Ma (Figure 7). Late Paleoproterozoic to Mesoprotero-
zoic dates, from 2137 to 1485 Ma, constitute the most com-
mon group of zircon ages in sample TR8 (37% of the
results; 40% of the concordant ages). The highest fre-
quency peak associated with this population is 1867 Ma
and no age gap of more than 100 Ma is found in the range
1926–1485 Ma. The second largest population is repre-
sented by Carboniferous and Permian ages between 327
and 277 Ma (25% of the results; 27% of the concordant
ages). One zircon yields a highly discordant age of 214
Ma. The Mesoproterozoic to late Proterozoic population,
represented by zircons of 1294–935 Ma, is also common
(16% of the results; 15% of the concordant ages). Four zir-
cons yielded Archean to early Paleoproterozoic ages
older than 2400 Ma.
In samples TR2, TR4 and TR6, the highest frequency
peaks in the probability density plots are Carboniferous
to Triassic (Figure 7). TR2 yielded 20 zircons dated
between 2392 and 243 Ma, of which 14 gave concordant
ages. The discordant ages range between 778 and 243 Ma.
The majority of the ages are Ediacaran–late Ordovocian
(16%) and late Paleozoic (53%). Samples TR4 (28 age
results) and TR6 (31 age results) are similar, having in
common the high proportion of discordant results, the
preponderance of upper Neoproterozoic (no Neoprotero-
zoic result older than 570 Ma) to Paleozoic zircon and the
occurrence of Triassic concordant ages (youngest ages of
244 and 218 Ma, respectively). The majority of the zircon
grains from TR4 yielded Carboniferous to Triassic ages
of 349–212 Ma (55%), although only four out of 12 gave
concordant ages. Sample TR6 is also enriched in Carbon-
iferous to Triassic grains (60% in the range 356–218 Ma).
The Paleo–Mesoproterozoic (1876–1576 Ma), Meso–Neo-
proterozoic (1098–964 Ma) and Ediacaran to middle Ordo-
vician (570–469 Ma) populations are distinguishable in
samples TR4 and TR6. Only six concordant ages, out of
11 measurements, were obtained from sample TR11. The
majority of the concordant ages belong to the Paleo–
Mesoproterozoic population.
In the northern and western Australian, margins out-
crop numerous rocks enriched in zircon ages comparable
to the 2150–1500 Ma, 1300–900 Ma and 630–460 Ma popula-
tions found in Timor stream sediments (e.g. Page Wil-
liams 1988; Collins Shaw 1995; Bodorkos et al. 1999;
Bruguier et al. 1999; Cross Crispe 2007; Fergusson et al.
2007; Rubenach et al. 2008). Zircons of these ages are also
present in other SE Asian areas that incorporate crustal
fragments that drifted away from the New Guinea–Aus-
tralia margin and accreted to the Eurasian plate during
the Cretaceous (Smyth et al. 2007; van Leeuwen et al.
2007; Clements et al. 2012; Hall Sevastjanova 2012).
Depending on the geological maps, the drainage area
for TR8 is entirely placed on the Aileu Formation/
Figure 5 Cathodoluminescence images of selected zircon
grains. Circles indicate position of SHRIMP analyses.
Figures preceded by ‘’ are discordant ages for a 10% cut-off.
Stream sediments, East Timor 515
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10. TAJE_A_810664.3d (TAJE) 17-07-2013 10:58
Complex (Audley-Charles 1968; Charlton 2002; Kaneko
et al. 2007) or spreads across the Maubisse Formation and
the Aileu Complex (Harris et al. 2000; Harris 2006). Both
units are included in the Gondwana Sequence of Timor.
In most works it is considered that the Aileu Complex is a
metamorphic complex that has higher metamorphic
grades in northern locations and interfingers southward
with the Maubisse Formation (Barber Audley-Charles
1976; Berry Grady 1981; Harris et al. 2000). As expected,
sample TR8 displays a zircon age signature comparable
to the Aileu Complex, in which Paleo–Mesoproterozoic
and Carboniferous–Permian grains form prominent
age clusters (Harris 2006; Hall Sevastjanova 2012). The
Carboniferous to Permian zircons from TR8 must be
genetically related with magmatism associated with
the break-up and northward drift of crustal blocks from
the northern Gondwanaland (e.g. Audley-Charles 1983;
Metcalfe 1998).
Except for the TR8 sampling point, the catchment
areas extend differently across units of the Banda Ter-
rane and Gondwana and Australian Passive Margin
sequences and syn- to post-orogenic sediments (Table 1).
In terms of zircon age signatures, the main differences
between TR8 and the other samples are the absence of
Triassic concordant results in the 365–210 Ma popula-
tion, the higher proportion of 2150–1500 Ma population
and the lower frequency of discordant zircons in the
former (Figure 7). The Triassic basic volcanic rocks of
the Gondwana Sequence (namely from the Maubisse
Formation) are expected to have limited zircon produc-
tivity so that other sources may be considered for the
younger ages in samples TR2, TR4, TR6 and TR11.
These zircon grains could be in part associated with
the felsic magmatism observed in Banggai-Sula Islands
(Pigram et al. 1985; Garrard et al. 1988) and Bird’s Head
(Pieters et al. 1983), two areas of the Sula Spur that
presently lie some 800 km north and 1000 km north-
west, respectively. Crustal fragments and respective
sedimentary cover from these regions were probably
carried south as the Australian continent advanced
northward and the subduction hinge rolled back south-
wards (Spakman Hall 2010; Hall 2012). It is then pos-
sible that rocks yielding Triassic zircon derived from
northern areas with Australian basement and were
entrained in Timor during and after the Miocene with
the thrust sheet emplacement of the allochthonous
complexes. The hypothesis that some metamorphic
complexes from Timor are associated with Australian
basement has been proposed by several authors
(Grady 1975; Grady Berry 1977; Harris Long 2000;
Charlton 2002).
Previous research on the Banda Terrane revealed
upper Cretaceous zircons in metasediments from the
Bebe Susu Massif (Standley Harris 2009) and late
Eocene zircons in an unmetamorphosed dacite from
West Timor (Harris 2006). These zircon ages were not
found in the studied stream sediments, which is not sur-
prising since the zircon productivity of the crystalline
rocks of the Banda Terrane is expected to be small when
compared with the more felsic units associated with the
Gondwana margin.
Numerous previously published age results from the
metamorphic complexes of Aileu, Bebe Susu (Harris
2006) and Lolotoi (Standley Harris 2009) are discor-
dant. Zircon age discordance may be due to the presence
of 204
Pb, loss of Pb at some time owing to a relevant geo-
logical disturbance (metamorphism) or because of abla-
tion of distinct zircon generations. Although ablation
pits created with SHRIMP II ion microprobe are subs-
tantially shallower than with laser ablation ICP-MS,
Figure 6 Histogram and probability density curves with valid U–Pb age results of zircon grains. Major populations are
highlighted. Measurements with 90–110% concordance are represented in histogram and by a dark grey probability density
curve. Bins on the histogram are 25 Ma.
516 P. A. Dinis et al.
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11. TAJE_A_810664.3d (TAJE) 17-07-2013 10:58
implying lower risk of discordance, the results obtained
during the present research also gave a substantial num-
ber of discordant ages. Given the lower proportion of dis-
cordant ages in TR8, which is entirely sourced by
Permian to Triassic rocks of the Gondwana Sequence,
one can assume that part of the remaining units were
influenced by some geological events responsible for Pb
loss that did not affect the Gondwana Sequence. The pre-
cise ages of these events cannot be resolved from the
available data.
CONCLUSIONS
The sampled stream sediments revealed that the units
exhumed in Timor have widely variable composition,
comprising rocks of mafic and felsic nature formed in
distinct tectonic settings. The contribution of different
source units associated with continental margin and
island arc settings is demonstrated by several geochemi-
cal data including the REE patterns and some ratios of
trace, minor and major elements.
Although the geology of the source units is variable,
the zircon signature is fairly homogeneous. No sampled
zircon is younger than Triassic and the most common
populations in all samples are 2150–1500 Ma and 365–210
Ma, followed by 1300–900 Ma and 630–460 Ma. The abun-
dance of discordant grains is also a relevant feature.
Sediments entirely sourced by the Gondwana Sequence
display a higher proportion of the 2150–1500 Ma popula-
tion, do not have Mesozoic zircon and contain a lower
proportion of discordant ages than those that include
material derived from both Australian and Asian affin-
ity units. The presence of material from the Sula Spur
may explain the homogeneity in the zircon age distribu-
tions, the presence of Triassic zircon in the younger pop-
ulation and the frequency of discordant results. Crustal
fragments from the Sula Spur that were carried south-
wards as the island arc progressed towards the Austra-
lian continent, and were emplaced with oceanic crust
and their sediment cover in Timor with the Banda
Terrane nappes, are likely to have a zircon signature
comparable to the Gondwana Sequence, but with nume-
rous Triassic grains.
Figure 7 Synthesis of geochemistry discriminant results and probability density curves of zircon age data. Discordant results
crossed concordia within error. Pie diagrams indicate the tectonic setting obtained from the geochemical data (as presented
in Figures 2 and 3). ACM, active continental margin; CIA/A-Ev, continental island arc or evolved arc setting; OIA/A-AD, Oce-
anic Island arc or arc setting with basaltic and andesitic detritus.
Stream sediments, East Timor 517
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12. TAJE_A_810664.3d (TAJE) 17-07-2013 10:58
ACKNOWLEDGEMENTS
Project SFRH/BSAB/1233/2011 from the Portuguese
Foundation for Science and Technology (FCT) and an
Iberoamerican Santander grant provided funding for
the laboratory work at University of S~
ao Paulo. Field-
work in East Timor and the geochronology data were
obtained during a sabbatical leave of PAD from Univer-
sity of Coimbra. K. Sato is acknowledged for the help
with SHRIMP analysis and interpretation of the geo-
chronology data. P. Pinto, S. Barrios, N. Almeida and R.
Danielsen kindly helped in the data acquisition and
preparation of the manuscript. The article benefited
from the critical reviews and valuable comments of R.
Hall and R. Berry.
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SUPPLEMENTARY PAPERS
Appendix 1 Composition of floodplain
Sediments
Appendix 2 U–Pb data of detrital zircon from
timor stream sediments
Stream sediments, East Timor 519
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