Oligocene Strata in the South Sistan Suture Zone, Southeast Iran: Implications for the Tectonic Setting

RESEARCH

Detrital zircon and provenance analysis of Eocene– Oligocene strata in the South Sistan suture zone, southeast Iran: Implications for the tectonic setting

Ali Mohammadi, Jean-Pierre Burg, and Wilfried Winkler DEPARTMENT OF EARTH SCIENCES, ETH ZURICH, SONNEGGSTRASSE 5, 8092, ZURICH, SWITZERLAND

ABSTRACT

The north-south–trending Sistan suture zone in east Iran results from the Paleogene collision of the Central Iran block to the west with the Afghan block to the east. We aim to document the tectonic context of the Sistan sedimentary basin and provide critical constraints on the closure time of this part of the Tethys Ocean. We determine the provenance of Eocene–Oligocene deep-marine turbiditic sandstones, describe the sandstone framework, and report on a geochemical and provenance study including laser ablation–inductively coupled plasma–mass spectrometry U-Pb zircon ages and 415 Hf isotopic analyses of 3015 in situ detrital zircons. Sandstone framework compositions reveal a magmatic arc provenance as the main source of detritus. Heavy mineral assemblages and Cr-spinel indicate ultramafic rocks, likely ophiolites, as a subsidiary source. The two main detrital zircon U-Pb age groups are dominated by (1) Late Cretaceous grains with Hf isotopic compositions typical of oceanic crust and depleted mantle, suggesting an intraoceanic island arc provenance, and (2) Eocene grains with Hf isotopic compositions typical of continental crust and nondepleted mantle, suggesting a transitional continental magmatic arc provenance. This change in provenance is attributed to the Paleocene (65–55 Ma) collision between the Afghan plate and an intraoceanic island arc not considered in previous tectonic reconstructions of the Sistan segment of the Alpine-Himalayan orogenic system.

LITHOSPHERE; v. 8; no. 6; p. 615–632; GSA Data Repository Item 2016316 | Published online 14 October 2016 doi:10.1130/L538.1

INTRODUCTION rocks were reworked from the growing accre- We combine results from field work, sand- tionary wedge related to convergence between stone framework compositions, and heavy The Sistan suture zone (SSZ) is a critical Arabia and Eurasia (e.g., Critelli et al., 1990; mineral analysis to characterize the lithologies link between the Himalaya and Zagros oro- Kassi et al., 2013; Qayyum et al., 2001). Carter eroded in the source areas and to constrain the genic belts and is a significant yet poorly stud- et al. (2010) suggested that Eocene–Oligocene tectonic setting and evolution of this part of the ied region in our understanding of the tecton- sandstones of the South Sistan Basin were sup- Sistan area. More than 3000 U-Pb ages of detri- ics of the Middle East and Central Asia. This plied from the Himalaya by the paleo–Indus tal zircon obtained by laser ablation–inductively study presents new heavy mineral, sandstone delta–submarine fan complex. coupled plasma–mass spectrometry are used to petrography, and zircon U-Pb and Lu/Hf data Sandstone framework analysis and heavy evaluate crystallization ages of the source rocks. that provide important information on the paleo- minerals studies are the main and classic tools of Hf isotope ratios of ~400 dated zircon grains are geographic and paleotectonic configuration of provenance analysis (e.g., Weltje and von Eynat- used to infer the origin of magmas in the source the region in the Eocene–Oligocene. This work ten, 2004), which provides valuable information region. Only a few studies have addressed both aims to reconstruct the Mesozoic and Ceno- on the composition of source rocks and, conse- detrital zircon geochronology and Hf isotope zoic geological history of the South Sistan quently, the past tectonic setting (e.g., Dickinson, data of Iranian sedimentary successions and plu- Basin, located north of the Makran accretion- 1985; Dickinson and Suczek, 1979; Zuffa, 1985). tonic rocks (e.g., Mohammadi, 2015; Moham- ary complex; we argue for a revised collision Among heavy minerals, zircon plays an impor- madi et al., 2016a, 2016b; Nutman et al., 2014). age between the Lut and Afghan blocks, which tant role because it is resistant to physical and Therefore, the large new data set of this study are of regional tectonic significance (Figs. 1–3). chemical processes (DeCelles et al., 2007; Geh- will help in our understanding of the Cenozoic We challenge a current hypothesis that detri- rels et al., 2011); in addition, zircon U-Pb geo- tectono-sedimentary evolution of southeast Iran tus from the Sistan Basin was derived from the chronology reliably determines crystallization in the larger regional context. Our results sug- Himalaya-Tibet region. ages of individual detrital grains (e.g., Košler gest that the detrital material in the South Sistan It has been suggested that Paleogene sedi- et al., 2002; Veiga-Pires et al., 2009). Measure- Basin is mostly derived from Late Cretaceous ments of Makran and adjacent basins were sup- ment of the Hf isotope in dated zircon grains oceanic island arc and Eocene–Oligocene tran- plied from the Himalaya by the paleo–Indus further enables characterization of the isotopic sitional continental arc sources, with minor con- River and deposited in a delta–submarine fan composition of the magma in which the zircons tributions from ophiolitic rocks. These sources complex, whereas Miocene to recent sedimentary crystallized (e.g., Sláma et al., 2008). can be tentatively related to equivalents of the

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includes a deformed accretionary wedge and a 60 62 64 flanking forearc basin. It consists of three tec- 50°E 60°E tonostratigraphic complexes separated by thrust faults (Camp and Griffis, 1982; Tirrul et al., 36°N 1983; Fig. 1). The Ratuk complex to the east is an older accretionary wedge that formed prior to IRAN Maastrichtian time. It is a narrow, dense tectonic 33 imbrication zone and comprises Cretaceous Birjand 28°N ophiolitic mélanges, metamorphic rocks including eclogites, blueschists, and epidote amphib- olites (Bröcker et al., 2013; Zarrinkoub et al.,

R a 2012), and sedimentary rocks including lower t u Helmand (Afghan) Block k Cretaceous limestone, upper Cretaceous turbid-

C o itic sandstones, Eocene nummulitic limestones, m p and Neogene conglomerates (e.g., Bröcker et le AFGHANISTAN Nehbandan x al., 2013; Fotoohi Rad et al., 2005; Tirrul et al., 1983). Multimethod dating (Rb-Sr, 40Ar/39Ar, and U-Pb) of metamorphic rocks yielded an age Lut sub-block of the of metamorphism between 87 and 81 Ma, which S e Central Iran Block indicates tectonothermal activity during the Late d a b Cretaceous (Bröcker et al., 2013). The Neh com- e v h 31 C s plex to the west is a fold-thrust belt consisting o v v m v v p askohv Hill of upper Cretaceous allochthonous ophiolites, Zahedan lex v -R v v low-grade metamorphic rocks, shallow-water v v Chagaiv v limestone, Eocene–Oligocene deep-marine turbiditic sandstones, and Eocene–Oligocene intrusions attributed to final suturing in the northern SSZ (Camp and Griffis, 1982; Mohammadi et al., 2016a; Pang et al., 2012; Tirrul et al., 1983; N Zarrinkoub et al., 2012). The Sefidabeh forearc Eocene-Oligocene eh plutonic intrusions A complex unconformably covers both the Neh cc re t and Ratuk complexes. It comprises an 8-km- Thrusts io n Saravan a thick, essentially clastic and volcanoclastic ry C sequence of Cenomanian–Eocene sedimentary om ge p lan lex rocks including both deep- and shallow-marine kra Mé 29 Ma n Ophiolitic limestones and calc-alkaline volcanic intercala- tions on the eastern side (Tirrul et al., 1983). Makran This association represents the piggy-back Accretionary Complex forearc basin that formed on the wedge during pre-Oligocene deformation (Tirrul et al., 1983). Strike-slip faulting and thrusting has generally IRAN PAKISTAN 100 km overprinted the stratigraphic, basal onlap onto the underlying wedge turbidites (Mohammadi, 2015; Tirrul et al., 1983). Figure 1. Major geological subdivisions of the Sistan suture zone (adapted from Mohammadi et al., The study area is located in the southern 2016a). Study area is shown. part of the SSZ, in the Neh complex, and covers parts of the area described in the Narreh-Now, Saravan, Pishin, Khash, Iranshahr, and Nikshahr Chagai–Raskoh Hills arcs and ophiolites to and was overprinted by subsequent dextral 1:250,000-scale geological maps (Figs. 1 and 4; the northeast, in neighboring western Pakistan strike-slip faulting between the Central Iran Eftekhar Nezhad and McCall, 1993; Eftekhar (Figs. 1–3). and Afghan blocks (Tirrul et al., 1983). Zircon Nezhad et al., 1995; Morgen et al., 1979; Sahandi U-Pb ages (113 and 107 Ma) of leucogabbros of et al., 1996; Samimi Namin et al., 1994, 1986). GEOLOGICAL SETTING the Birjand ophiolites in northwest Sistan indi- Some interpret the southern Neh complex as a cate that this oceanic basin already existed in transitional zone between the Sistan and Makran The north-northwest–south-southeast–trend- Aptian time (Bröcker et al., 2013; Zarrinkoub Basins (e.g., Carter et al., 2010; McCall, 2002). ing SSZ in east Iran separates the continental et al., 2012). An eastward dip direction of the This area is principally composed of Eocene and Lut subblock of central Iran to the west from related subduction is inferred from paleogeo- Oligocene deep-marine turbidites, as indicated the Afghan block to the east (e.g., Şengör, 1990; graphic, structural, and petrographic consider- by presence of, e.g., Paleodictyon and Spirorha- Figs. 1 and 3). The Sistan Ocean was a branch of ations (e.g., Camp and Griffis, 1982; Moham- phe involute ichnofossils (Fig. 5; Crimes and the Tethys Ocean that closed in the late Eocene madi et al., 2016a; Tirrul et al., 1983). The SSZ McCall, 1995; Shabani Goraji, 2015), and their

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Caspian A Sea Tarim Basin

Pamir

H UDVB er t Fault Z a ag Sa-Si-Z ro Central Iran s Tibet Fo ld Block Afghan an CHF d Block T h SSZ KB ru st B SFTB e lt Himalayas (Fig. B) MF JD MD Persian Ch-Ra Gulf MAW O man Subductio n OOB Indian Shield Arabian Shield Arabian Sea Bay of Bengal Shyok Suture Kohistan-Ladak Complex Trans-Himalayan Batholith

? Indus-Tsangpo Suture Tethyan sedimentary Zone High Himalayan Metamorphic Belt fen Lesser Himalayan Zone Sub-Himalayan foreland Basin

B ~ 500 km

Figure 2. (A) Simplified tectonic map of the potential source terranes. Abbreviations: CHF—Chaman fault; Ch-Ra—Cha- gai-Raskoh arc; JD—Jaz Murian depression; KB—Katawaz Basin; MAW—Makran accretionary wedge; MF—Minab fault; OOB—Oman Ophiolite Belt; SFTB—Sulaiman fold-thrust belt; Sa-Si-Z—Sanandaj-Sirjan zone; SSZ—Sistan suture zone. Hachured area in SSZ indicates study area. (B) Simplified tectonic map of the south Tibet–Himalayan regions with potential sources discussed in the text. Figure and caption modified from Mohammadi et al. (2016b).

Nain-Baft Ocean Central Iran Block Sistan Sanandaj-Sirjan Zone Ocean Afghan Block Figure 3. Paleogeographic map of the Sistan Ocean including microcontinental blocks and subduction zones during the Zagros Eocene (modified from McCall koh et al., 1985). s as ubduction zone rc Chagai-Rnic a volca Kuh-e-Birk South Sistan Basin Fannuj Ocean Carbonate platform

Makran subduction zone

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e istan k Pa e t e Oligocene - 63°15' y

ocene ty

urbiditic calcareous sandstone urbiditic shale and sandstone urbiditic sandstones and shal

Samples Ci Thrusts Quaternar Late Eocene Eocene Cretaceous Pliocene Mi Ophiolites Granite T T Coloured Mélange Andesite and basal Limestone Metabasic volcanics Meta sandstones and metabasic schists Slate and phyllitic shal T Marbl e Olistostrom e Conglomerat E`

63°00'

3 N 6°

62°45' 60°E 252 260 246 135 263 AN IR 62°30'

50°E van

123 Sara D

28°N —Shirinzad unit. ′ —Shirinzad C` 280 62°15' 124 218 62°00' istan 237 k

Pa 97 C E-E ′ —Badamu-Siahan unit; 224 293 61°45'

105

206 A` 61°30' —Saravan unit; D-D unit; ′ —Saravan 94 186 166 Khash 61°15' 157 —Kaskin unit; C-C ′ —Kaskin unit; 61°00'

134 B` 60°45' —East Iran flysch; B-B flysch; ′ —East Iran A anshahr

' 29°00 28°15' ' 28°00 28°45' 28°30' 26°45' 27°15' 27°00' 27°30' 27°45' 60°18' Figure 4. Simplified geologic map of the South Sistan Basin. Stratigraphic ages according to the 1:250,000-scale geological maps of Pishin, Narre-Now, Saravan, Khash, Iranshahr, and Iranshahr, Khash, Saravan, Narre-Now, to the 1:250,000-scale geological maps of Pishin, according ages Stratigraphic geologic map of the South Sistan Basin. Simplified 4. Figure stratigraphic Location of 1986). 1994, al., Samimi Namin et 1996; Sahandi et al., 1979; et al., Morgen 1995; et al., Nezhad Eftekhar 1993; McCall, Nezhad and Eftekhar 2010; (Dolati, Makran A-A 6: sections in Figure

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A B

C D

E F

Figure 5. Trace fossils of Eocene deep-marine turbidites of the Neh complex. (A) Spirorhaphe involute. (B) Nereiles jacksoni. (C) Taphrhelmintopsis auricularis Sacco. (D) Paleodictyon carpathicum. (E) Helminthoida crassa. (F) Helminthoida ichnosp.

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MOHAMMADI ET AL.

Eocene Oligocene Pliocene iocene M

ddle Mi Late Early Early Late 5. 3 28. 4 40. 4 55. 8 23. 0 33. 9 48.6 94 10 5 13 4

Gravel n

ilt S in Unit 12000 m ask K 200 0 m 400 0 m 800 0 m 600 0 m 12000 m 10000 m

26 0 25 2 28 0

Gravel n

a S eave s

t Silt acks/trails paleo current vector 8443 m Convolute Lamination Tr Burrow sL Shirinzad Uni 600 0 m 200 0 m 400 0 m 800 0 m n

15 7 16 6

Gr n Sa

ysch s Silt Fl 1100 m Flute cast s Ripple cross lamination Climbing ripple cross laminatio Load Cast East Iran 6000 m 2000 m 8000 m 4000 m 1000 0 m

263 186 124 218 224

Gravel

Sand Silt van Unit 6850 m Sara 4000 m 2000 m 6000 m

246 135 293 237 206 123

Sample number avel

Sand Silt Unit 13000 m Badamu-Siahan Unit 6000 m 4000 m 2000 m 8000 m 10000 m 12000 m

5.3

23. 0 28. 4 33. 9 40. 4 48. 6 55. 8

ddle Mi Late Early Early (Ma) Late

Oligocene Eocene Pliocene iocene M Epoch the Zaboli unit in to Badamu-Siahan unit is equivalent and sampling locations. directions section of the South Sistan Basin with paleocurrent stratigraphic Composite 6. Figure unit flysch the East Iran to unit is equivalent The Saravan Badamo unit in the 1:250,000-scale the Kuh-e map of Narreh-Now. and to geological 1:250,000-scale map of Saravan geological to and the Kaskin unit is equivalent the Mashkid unit in 1:250,000-scale to map of Saravan, geological unit is equivalent The Shirinzad in the 1:250,000-scale map of Khash. geological of Iran. the Geological Survey maps published by All cited the Rask unit in 1:250,000-scale map of Pishin. geological

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very low-grade metamorphic equivalents such South Sistan paleocurrents N 56 measurements distances from source to sink. U-Pb dating of as slate and phyllite. These turbiditic sequences detrital zircons was done on 17 Eocene–Oligo- were subdivided into nine lithostratigraphic units cene sandstone samples (Figs. 10–13). Ages with (typically as thick as several hundred meters) that discordance >5% are not included. Zircon ages are dominated by Bouma-type turbiditic sand- older than 1100 Ma were not plotted due to their stones and shales (Eftekhar Nezhad and McCall, rarity. Cretaceous and Eocene ages prevail with 1993; Eftekhar Nezhad et al., 1995; Morgen et Cretaceous peaks at 106, 89, and 68 Ma and an al., 1979; Sahandi et al., 1996; Samimi Namin Eocene peak at 49.5 Ma (Figs. 10–13). Zero to et al., 1994, 1986; Fig. 6). Most sandstones are very short lag time (i.e., Eocene zircons hosted feldspathic litharenites and lithic arkoses, and in sandstone of similar stratigraphic age) indi- contain assemblages of planktonic and benthic cates synsedimentary magmatism in the source foraminifera and nannofossils (Table S1 in the area (Fig. 14). Data Repository1; McCall et al., 1985). Depending on the size of zircon grains and their texture (internal growth structure and inclu- METHODS AND SAMPLES sions imaged by cathodoluminescence and backscattered electron imaging), Hf isotope ratios We investigated 20 medium-grained turbiditic were measured on dated zircons (Woodhead et

sandstones (with prefix 12 a.m. and 13 a.m. in the Figure 7. Rose diagram of paleocurrent measure- al., 2004). The evolved epsilon hafnium (eHf(t)) ETH Zurich collection) from 5 lithostratigraphic ments from 53 flute cast and 3 asymmetric ripple time-corrected data from zircons older than units of the Neh complex (Figs. 4 and 6; Table marks from 53 outcrops restored to horizontal 600 Ma are not shown in Figure 10. Late Cre- S2). For nannofossil determinations, samples around the local strike of bedding. Arrow indi- taceous zircon grains show a large variation in cates average direction. were taken from hemiplegic sediments of tur- eHf(t), from -17 to +20.4. Most range between

biditic sequences to avoid reworked nannofossils. eHf(t) = 0 and +20.1; a few range between 0 Pelagic nannofossils confirmed the mapped stra- and -17 (Fig. 15). Zircons with Eocene ages

tigraphy, suggesting sedimentation ages ranging Similar Lv:Ls ratios indicate magmatic arc prov- have eHf(t) values between +16 and -24, a large from Eocene to Oligocene (Table S1). Analytical enance rather than recycled orogen suites (Fig. majority between 0 and +15, and a few with methods, including mineral separation and iden- 6D). The sources plot mostly in the recycled negative values (Fig. 15). Compared to the upper tification techniques, are described in Appendix 1. orogenic field (Fig. 8E), more precisely in the Cretaceous zircons, Eocene zircons show less

field of dissected arcs (Fig. 8F). positive εHf(t) between the (CHUR) and depleted

RESULTS mantle lines (Fig. 15). Negative εHf(t) indicate Heavy Minerals magmatic zircons with a continental crust sig-

Paleocurrents nature whereas positive εHf(t) values indicate Heavy mineral suites show very variable depleted mantle signatures (e.g., Naing et al., Paleocurrent directions were measured from compositions and can be subdivided into four 2014; Patchett, 1983). 53 flute casts and 3 asymmetric ripple marks of groups: (1) most stable minerals (zircon, tour- 53 outcrops from different parts of the South Sis- maline, rutile [ZTR], monazite, brookite, and DISCUSSION tant Basin Neh complex. Readings were rotated anatase; ZTR = 75%–65%) and apatite derived to horizontal around the local strike direction from continental crust sources; (2) variably abun- Taken together the new sandstone frame- of bedding. Measurements indicate a regional dant (4%–70% of 200 counted grains) less stable work composition, heavy mineral, U-Pb geo- northeast to southwest paleoslope with a source minerals (epidotes, garnet, staurolite, chloritoid, chronology, and Hf isotope data for Eocene– area to the northeast of the basin (Fig. 7). kyanite, andalusite) suggesting different detrital Oligocene sandstones of the South SSZ allows sources of medium-grade metamorphic rocks; for refining evolutionary models of the southern Modal Framework Composition (3) Cr-spinel (to 20% of total grain count) and part of the Sistan segment of the Asian Tethyan very small amounts of serpentine indicating sutures. The studied sandstones classify mainly as contributions from exhumed ultramafic rocks; The main hypothesis previously put forward lithic arkose and feldspathic litharenite (Fig. 8A). (4) pyroxenes (diopside, enstatite, ferrosilite, and for the provenance of the South Sistan Basin Quartz grains are mostly monocrystalline (82%), hedenbergite) from basic to intermediate mag- sandstones is that these deposits were derived and feldspar is dominantly plagioclase (>91%) matic rocks (Fig. 9). Lower-middle Eocene sand- from the Himalayas in the paleo–Indus delta– with minor amounts of K-feldspar (Fig. 8B). stones (samples 123, 157, 186, and 237) gener- submarine fan (Katawaz Delta) and transported Lithic fragments are represented by sedimentary ally show large amounts (to 80% of total grain further westward into the Khojak submarine fan (Ls), volcanic (Lv), and metamorphic clasts (Fig. count) of epidotes and pyroxenes. Oligocene and Makran–South Sistan Basins accretionary 8C). Volcanic rock fragments are mostly andes- sandstones (samples 97 and 105) yielded large wedges (e.g., Carter et al., 2010; Ellouz-Zim- ite and volcanic glass. Sedimentary lithic frag- amounts (to 87% of total grain count) of garnets, mermann et al., 2007; Kassi et al., 2003). Com- ments include mainly siltstone and limestone. epidotes, and pyroxenes (Fig. 9). parison of U-Pb ages and Hf isotopic composi- Metamorphic lithic grains generally consist of tions of the studied detrital zircons with those low-grade to medium-grade phyllites and schists. Detrital Zircon Dating and Hf Isotope in Himalaya Eocene–Oligocene sandstones Geochemistry (the Indus suture molasses, Kailas Basin, Sulai- man fold-thrust belt, and Katawaz Basin) and 1 GSA Data Repository Item 2016316, Tables S1–S6, is available at www.geosociety.org/pubs/ft2016.htm, Most detrital zircon crystals (85%) are magmatic zircons of the Karakoram, Kohistan- or on request from [email protected]. euhedral to anhedral, suggesting short transport Ladakh arc and Zahedan-Shah Kuh plutonic belt

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Q Qm quartz sandstone Oligocene Late Eocene subarkose sublitharenite Middle Eocene Early Eocene

Literature data 105 280 AB97 218 124 246 206 263 224 237 166 293 293 123 134 157 97124 94 252 218 157 186 246 263 224 280 135 123 166 252 105 134 237 135 94 186

206

lithic feldspathic arkose arkose litharenite litharenite FLPK Lvh Qp

Q: total quartzous grains Qm: monocrystalline quartz 206 Qp: polycrystalline quartz L: non-quartzeous lithoclasts Lt: total lithoclasts 186 Lvh: volcanic/hypabyssal lithoclasts Ls: sedimentary lithoclasts CDLm: metamorphic lithoclasts P: plagioclase K: K-feldspar 218 237 F: total feldspar 224 246 166 135 252 134 157 124 97 280 157 263 293 293 123 105 124 94 134 123 166 97 224 280 94 218 237 135 186 263 206 246 252 105

Ls Lm Lvh Ls Q Qm

craton craton interior interior

quartzose recycled transitional transitional continental

EFcontinental recycled orogenic

293 97124 mixed transitional 218 157 recycled 263 224 246 218 166 280105 123 252 293 134 97 237 263 124 105 135 224 246 166 dissected 123 252 94 dissected 134 237 arc 157 280 basement 186 basement arc 94 135 uplift uplift lithic 186 recycled transitional arct206 ransitional arc 206 undissected arc undissected arc FLFLt Figure 8. Detrital composition and classification of the South Sistan sandstones in provenance ternary diagrams. (A) Sandstone classification diagram (Folk, 1980). (B) Qm-P-K diagram (after Dickinson and Suczek, 1979). (C) Lvh-Ls-Lm diagram (after Dickinson, 1985). (D) Qp-Lvh-Lsm diagram (after Dickinson and Suczek, 1979). (E) QFL (Dickinson, 1985). (F) QmFLt (Dickinson, 1985). Literature data from the middle Eocene–early Miocene Khojak Formation in the Katawaz Basin are from Qayyum et al. (2001).

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12 AM 105 12 AM 97 Zircon, Monazite

Oligocene 12 AM 134 Tourmaline 13 AM 280 Rutile, Brookite, Anatase, Sphene 13 AM 252 Spinel 13 AM 260 Apatite

Late Eocene 13 AM 263 Epidote group 12 AM 124 Garnet 13 AM 246 Hornblende 12 AM 135

iddle Eocene Amphibole 13 AM 293 13 AM 218 Pyroxene group Staurolite eM 13 AM 224 13 AM 166 Chloritoid 13 AM 206 Kyanite 12 AM 123 AAndalusite 13 AM 237 Others Early - Middle Eocen 13 AM 157 13 AM 186 0% 20%40% 60%80% 100% Figure 9. Heavy mineral assemblages of the South Sistan Basin sandstones arranged in stratigraphic order and showing the relative abundance of heavy mineral groups. Cretaceous Jurassic Pe Carboniferous Dev Silurian Ordovician Cambrian Neo 1200 Tr iassic rmian onian Pr South Sistan Basin 1100 89 oterozoic n=3015

1000 49.5 900

800

Figure 10. Zircon U-Pb age 700 distribution pattern of all sandstone samples from the 600 South Sistan Basin. Time scale is after Gradstein et 500 al. (2012).

400

300

200

100

0 0 100 200 300 400 500 600700 800900 1000 1100 U-Pb Age (Ma)

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Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/8/6/615/3050732/615.pdf by guest on 26 September 2021 MOHAMMADI ET AL. Cretaceous Cretaceous Tr Jurassic Pe Car De Silurian Ordovician Cambrian Neo Pr Jurassic Pe Car Dev Siluria Ordovician Cambrian Neo Pr Tr iassic iassic rmia 90 rmia 120 vonian boni fe bonif Sample 13 AM 186 onian Sample 13 AM 206 88.7

87.8 n oterozoic oterozoic n Eocene (Ypresian-Lutetian) n Eocene (Ypresian-Lutetian) erou

80 rous

n=162 zircons, 5>1100 Ma n=247 zircons, 10>1100 Ma s Youngest 42.9 ± 0.92 100 Youngest 40.73 ± 0.62 70 0.14 0.20 U

U 1100 38 60 0.12 80 38

/ 700 / 0.16

Pb 900 Pb 50 48.6 0.10 20 62 48.8 20 62

0.08 500 60 0.12 700 69 40 Number Number 0.06 0.08 500 300 30 40 0.04 107.8 300 0.04 20 0.02 100 2072Pb/ 35U 20 100 207Pb/235U 0.00 0.00 10 0.00.2 0.40.6 0.81.0 1.2 0.00.4 0.81.2 1.62.0 2.42.8

0 0 0 100 200 300 400 500 600 700 800 900 1000 1100 0100 200300 400500 600700 800900 1000 1100 Cretaceous Jurassic Tr Pe Car Dev Siluria Ordovician Cambr Neo Pr Cretaceous Tr Jurassic Pe Car Dev Silurian Ordovician Cambrian Neo Pr iassi c iassic rmia rmian bonif bonif

60 onian Sample 13 AM 166 onian Sample 13 AM 157 n oterozoic ian oterozoic 35 n Eocene (Ypresian-Lutetian)

50.4 Eocene (Ypresian-Lutetian) erou erou 67.8

n=131 zircons, 0>1100 Ma n=126 zircons, 4>1100 Ma s 50 88.8 s Youngest 33.07 ± 0.48 Youngest 45.57 ± 0.8 30

106.5 U

U 0.20 0.20 238 1100 / 40 238 1100 25 / Pb 0.16 0.16 Pb 900 900 206

206 20 47 30 0.12 700 0.12 700 Number Number 500 15 0.08 0.08 500 20 300 0.04 300 10 0.04 207 235 100 Pb/ U 100 10 0.00 2072Pb/ 35U 0.0 0.20.4 0.60.8 1.01.2 0.00 5 0246

0 0 0100 200300 400500 600700 800900 1000 1100 0100 200300 400500 600700 800900 1000 1100 Cretaceous Cretaceous Jurassic Tr Pe Ca De Silurian Ordovician Camb Neo Pr Tr Jurassic Pe Car De Silurian Ordovician Cambr Neo Pr iassic iassi c rmia rbonif rmia vonia vonian 90 Sample 13 AM 123 bonif Sample 13 AM 218 rian

oterozoic 80 oterozoic ian n Eocene (Ypresian-Lutetian) 106.9 n n erou

erous Eocene (Ypresian-Lutetian) 80 89.3

n=176 zircons, 8>1100 Ma n=214 zircons, 11>1100 Ma s Youngest 42.5 ± 0.76 70 Youngest 37.57 ± 0.53 70 72.6 U 0.20 60 0.20 U 38 1100 38 1100

60 / 50.2 / Pb

0.16 50 0.16 Pb 900 900 50 20 62 20 62

0.12 700 40 0.12 700 40 Number Number 500 0.08 500 30 0.08 30 300 300 0.04 0.04 20 20 100 207Pb/235U 48.2 100 207Pb/235U 0.00 0.00 10 0.0 0.4 0.8 1.2 1.6 2.0 2.4 10 0.00.4 0.81.2 1.62.0

0 0 0100 200 300 400 500 600 700800 900 1000 1100 0100 200300 400500 600700 800900 1000 1100 206 Pb / 238 U age (Ma) 206 Pb / 238 U age (Ma)

Figure 11. Probability density diagrams for detrital zircon 206Pb/238U age populations with corresponding Concordia plots of concordant detrital zircons of samples 186, 206, 157, 166, 123, and 218 from South Sistan Basin sandstones. Ages with discordance >5% are not included. Time scale is after Gradstein et al. (2012).

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bonif Sample 13 AM 224 onian Sample 13 AM 237 oterozoic

88.9 oterozoic Eocene (Ypresian-Lutetian) n Eocene (Ypresian-Lutetian) erous erou 50 120 n=242 zircons, 4>1100 Ma n=94 zircons, 1>1100 Ma

88.8 s Youngest 45.3 ± 0.31 50.8 Youngest 40.51 ± 0.61 100 U 40 U 0.16 0.20 238

238 1100 / 900 / Pb

80 Pb 0.16 900 0.12 206 30 700 206 51.1 0.12 700 Number 60 0.08 500

Number 500 20 0.08

300 40 300 0.04 0.04

10 207235 100 2072Pb/ 35U 100 Pb/ U 20 0.00 0.00 0.00.4 0.81.2 1.62.0 2.4 0.0 0.4 0.8 1.2 1.6

0 0 0 100 200 300 400 500 600 700 800900 1000 1100 0100 200300 400500 600700 800900 1000 1100 Silurian Ordovician Cambr Neo Cretaceous Jurassic Tr Pe Carboniferous De Cretaceous Jurassic Tr Pe Carboniferous De Ordovician Cambrian Neo Silurian iassi c

90 iassic rmian rmian vo 90.9 Sample 13 AM 293 vo Sample 13 AM 246 Pr Pr

nian 89.6 nian oter ian Eocene (Lutetian) oter Eocene (Lutetian) 80 52.5 120 oz

n=178 zircons, 4>1100 Ma oz n=229 zircons, 7>1100 Ma

oic Youngest 45.49 ± 0.72 oi c Youngest 40.2 ± 0.36 70 100 U

U 69.5 0.20 0.20 238

60 238 1100 /

/ 1100 Pb

Pb 80 0.16 0.16

50 206 900 206 900

0.12 700 60 0.12 700

Number 40 Number

0.08 500 500 30 51 0.08 40 300 108.1 300 20 0.04 0.04

207235 100 Pb/ U 20 207 235 0.00 100 Pb/ U 10 0.0 0.40.8 1.21.6 2.02.4 0.00 0.00.4 0.81.2 1.62.0 2.4

0 0 0100 200300 400 500 600 700800 9001000 1100 0 100 200 300 400 500 600 700 800900 1000 1100 Cretaceous Silurian Ordovician Camb Neo Cretaceous Jurassic Tr Pe Carboniferou De Tr Jurassi Pe Carboniferous De Silurian Ordovician Cambr Neo iassic 90.4 iassic rmia rmia vo Sample 13 AM 135 vo Sample 13 AM 124 Pr Pr nian

100 nian rian 60 oter c 50.3 oter ian n Eocene (Lutetian) 89 n Eocene (Lutetian-Bartonian)

oz oz

n=184 zircons, 4>1100 Ma n=168 zircons, 2>1100 Ma oi c s oi c Youngest 42.19 ± 0.92 Youngest 42.1 ± 0.6 50 80 0.24 U U 0.20 38

238 1100

49.6 /

0.20 / 1100 40

67.4 Pb Pb 0.16 60 900

0.16 206 20 62 900

30 0.12 700 0.12 700 Number 40 Number 500 500 0.08 0.08 20 102.5 300 300 0.04 0.04 20 100 207Pb/235U 10 100 2072Pb/ 35U 0.00 0.00 0.00.4 0.81.2 1.62.0 2.4 0.0 0.40.8 1.21.6 2.0 2.4

0 0 0 100 200 300 400500 600700 800 900 10001100 0100 200300 400500 600700 800900 1000 1100 206 Pb / 238 U age (Ma) 206 Pb / 238 U age (Ma)

Figure 12. Probability density diagrams for detrital zircon 206Pb/238U age populations with corresponding concordia plots of concordant detrital zircons of samples 237, 224, 293, 246, 135, and 124 from South Sistan Basin sandstones. Ages with discordance >5% are not included. Time scale is after Gradstein et al. (2012).

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120 iassic rmian Sample 13 AM 263 48.6 vo Sample 13 AM 260 Pr nian 69.6 Eocene (Priabonian) 60 oter Eocene-Oligocene (Priabonian-Rupelian) erous n

oz n=157 zircons, 8>1100 Ma 100 n=184 zircons, 0>1100 Ma 87.2 Youngest 53.54 ± 0.62 oic Youngest 36.2 ± 0.47 50 0.24 0.018 110 U U

80 238

0.20 / 238

0.016 / 100 1100

40 Pb Pb 0.16 90 206 900

0.014 206 60 106 80 30 0.12 700 0.012 91 Number

70 Number 0.08 500 40 0.010 72 60 20 300 0.04 0.008 50 100 207Pb/235U 0.00 20 207Pb/235U 0.00.4 0.81.2 1.62.0 2.4 0.006 10 0.02 0.06 0.10 0.14 0.18 0.22

0 0 50 70 90 110130 150170 0100 200 300 400 500600 700 800900 1000 1100 Cretaceous Jurassi Pe Carbonif Dev Siluria Ordovician Cambrian Neo Tr Tr Cretaceous Jurassic Pe Carboniferou De Siluria Ordovician Cambrian Neo iassic iassic rmian rmian Sample 13 AM 252 vo

onian Sample 13 AM 280 Pr Pr nian n n c oter 50 Oligocene (Priabonian-Rupelian) 108.7 oter Oligocene (Priabonian-Rupelian) 47.9 erous 50 oz oz

n=144 zircons, 5>1100 Ma n=149 zircons, 3>1100 Ma oi c oic Youngest 40.2 ± 0.27 s Youngest 31.52 ± 0.35 40 0.20 49 U

U 1100 40 0.20

238 1100 238 / / 0.16 Pb

Pb 900 0.16 900 30 206 206 30 87 0.12 700 0.12 700 106.7 Number Number 71 500 500 0.08 20 0.08 20 300 300 0.04 0.04

10 10 100 207Pb/235U 100 207 235 0.00 Pb/ U 0.0 0.4 0.8 1.21.6 2.02.4 0.00 01234 5

0 0 0 100 200 300 400 500 600700 800900 1000 1100 0100 200300 400500 600700 800900 1000 1100 206 Pb / 238 U age (Ma) Cretaceous Jurassic Tr Pe Carbonif Dev Silurian Ordovician Camb Neo iassi c rmian

onian Sample 13 AM 134 Pr

80 rian 88 oter Oligocene (Rupelian) erou

n=152 zircons, 2>1100 Ma oi c 70 s Youngest 36.7 ± 1.01

48.5 0.16 900 60 U 238 /

50 0.12 Pb 700 r 206

40 500 0.08 Numbe 30 300 0.04 20 100 2072Pb/ 35U 0.00 10 0.00.4 0.81.2 1.6

0 0 100 200 300 400 500 600700 800 900 1000 1100 206 Pb / 238 U age (Ma)

Figure 13. Probability density diagrams for detrital zircon 206Pb/238U age populations with corresponding concordia plots of concordant detrital zircons of samples 263, 260, 252, 280, and 134 from South Sistan Basin sandstones. Ages with discordance >5% are not included. Time scale is after Gradstein et al. (2012).

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Sample No: 0 123 10 124 ) 134 Miocene 20 135 30 Olig . 157 40 166 186

Eocene 50 206 60

Pale. 218 70 224 237 80 246 90 252

Cretaceous 260

Mean age of zircon population (Ma 100 263 110 280 293 120 0 10 20 30 40 50 60 Miocene Oligocene Eocene Paleocene 5.3 23 33.9 55.8 Stratigraphic age of samples (Ma) Figure 14. Zircon mean U-Pb age populations versus stratigraphic age of sandstone samples. Time scale is after Gradstein et al. (2012). Paleo.—Paleocene; Olig.—Oligocene.

Sistan northern/central Lhasa belts Karakoram 25 Gangdese/TransHimalaya Kohistan Ladakh Island Arc Indus Molasse

15 Depleted Mantle

5 (t ) 0 CHUR ε Hf -5

-15

-25 0 50 100 150200 250 U-Pb age (Ma)

206 238 Figure 15. Time-corrected εHf(t) values versus U/ Pb zircon ages (Ma) of the South Sistan Basin sandstones and pub-

lished eHf(t) data of northern-central Lhasa belt, Karakoram batholith, Kohistan-Ladakh arc, Gangdese-Trans Himalaya, and Indus Molasse (Bouilhol et al., 2013; Heuberger et al., 2007; Ji et al., 2009; Ravikant et al., 2009; Wu et al., 2007; Zhuang et al., 2015). Age correction based on chondritic values (CHUR—chondritic uniform reservoir) from Blichert-Toft and Albarède (1997). Depleted mantle evolution trend (dashed line) is from Griffin et al. (2000). Time scale is after Gradstein et al. (2012).

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South Sistan Basin (n=3015) 89 Kailas Basin (n=503) Indus suture molasses (n=813)

49.5 Sulaiman Basin (n=823) Katawas Basin (n=314) Makran Accretionary Wedge (n=2924) Karakoram (n=739) Kohistan-Ladakh Arc (n=1858) 49.5 Gangdese Batholith (n=1372) 89 Tethyan Himalaya (n=1943) Lesser Himalaya (n=798)

Higher Himalaya (n=680)

020406080 100 120 140 160 180 200 U-Pb age (Ma)

0 0.5 1.0 1.5 2.0 2.5 3.0 3.5 U-Pb age (Ga) Figure 16. Normalized probability plots of South Sistan Basin strata, Kailas Basin (DeCelles et al., 2011), Indus suture molasse deposits (Henderson et al., 2010), Sulaiman fold-thrust belt (Zhuang et al., 2015), Gangdese batholith (Chu et al., 2006; Ji et al., 2009; Wen et al., 2008), Katawaz Basin (Carter et al., 2010), Makran accretionary wedge (Mohammadi, 2016b), Karakoram batholith and Kohistan-Ladakh arc (e.g., Fraser et al., 2001; Hon- egger et al., 1982; Jain and Singh, 2008; Krol et al., 1996; Parrish and Tirrul, 1989; Phillips et al., 2004; Ravikant et al., 2009; Schaltegger et al., 2002; Schärer et al., 1984; Singh et al., 2007; Upadhyay et al., 2008; Weinberg et al., 2000), Tethyan Himalayan strata, Lesser Himalayan strata, and Higher Himalayan strata (e.g., Gehrels et al., 2011). Figure and caption are adapted from Gehrels et al. (2011).

challenges the paleo–Indus delta–submarine fan significantly increases while the amount of Cr- and/or metamorphic source areas could be any- hypothesis (Figs. 15 and 16; Table 1). spinel decreases in the Oligocene sandstones. where after repeated reworking through several This implies that metamorphic rocks were more tectonic cycles since the Archean. Restricting Evidence from Heavy Mineral eroded than the ophiolite sources in late Eocene– conjecture to the closest continental blocks, in Assemblage Oligocene time. agreement with other euhedral grains indicating proximal source regions, points to the Cen- The heavy mineral spectrum indicates that Provenance of the Detrital Zircons tral Iran and the Afghan blocks in the western the Eocene–Oligocene lithic-rich arkoses and and eastern margins of the South Sistan Basin, feldspathic litharenites of the South Sistan The 3015 detrital zircon grains analyzed respectively. Zircon U-Pb age of magmatic, met- Basin region represent detritus from magmatic from the Eocene–Oligocene turbiditic sand- amorphic, and siliciclastic rocks of central Iran arcs (residual mantle signature), ophiolites stones yielded apparent ages ranging from ca. range from 1870 to 462 Ma with few Archean (Cr-spinel and serpentinite), and metamor- 3.3 Ga to ca. 31 Ma (Figs. 10–13). Three U-Pb zircon cores; the major population peak is

phic suites. (1) Cr-spinels have TiO2 contents age ranges broadly characterize the South Sistan between 547 and 525 Ma (Ramezani and Tucker, <0.2%, suggesting an ultramafic rather than a Basin detrital zircon grains. 2003). The southwestward paleocurrent direc- volcanic origin (Hu et al., 2014; Kamenetsky The oldest age range, represented by ≤5% of tions favor derivation from the Afghan block. et al., 2001). (2) Epidote and pyroxene may studied grains, dates from Archean (3.3 Ga) to Detrital zircon ages from the Himalayas and derive from exhumed ophiolite suites, meta- Jurassic (200 Ma). This age range does not make regions farther north range from 2.8 Ga to 95 Ma, morphic rocks or mafic to intermediate intrusive a single homogeneous spectrum, and Cambrian while Eocene detrital zircons are absent in sand- rocks. (3) Abundant metamorphic lithic grains zircons (540–480 Ma) are slightly more abun- stones of the Lesser Himalaya, Tethyan Hima- and metastable heavy minerals such as garnet, dant. The rounded and anhedral shape of zircon laya, and Greater Himalaya (e.g., Alizai et al., staurolite, and chloritoid represent metamorphic grains without internal growth zoning suggests 2011; DeCelles et al., 2000; Gehrels et al., 2011; rocks and metamorphosed sedimentary rocks that they are either fragments or old zircons Fig. 16). South Sistan Basin sandstones have as subsidiary sources (Deer et al., 1992). The reworked from continental crystalline rocks few Archean (to 3.3 Ga) detrital zircons older amount of metamorphic heavy minerals such or inherited magmatic zircons. The origin of than those of the Himalayan regions, and the as garnet, pyroxene, amphibole, and epidote these old grains is uncertain. Possible igneous main age populations are Late Cretaceous and

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TABLE 1. COMPILATION OF PROVENANCE INDICATORS FROM MAGMATIC ARCS AND CONTEMPORANEOUS SEDIMENTARY BASINS IN THE HIMALAYAN SYSTEM AND MAKRAN ACCRETIONARY WEDGE

Potential sources Sandstone modal framework Heavy minerals Zircon U-Pb age Hf isotopic composition εHf(t) References area Kailas Basin dominant volcanic and absence of Cr-Spinel younger than 100 Ma (19.5% of –DeCelles et al. (2011) sedimentary lithics zircons older than 100 Ma) main peaks ca. 24–26 Ma; 48 Ma; 75–80 Ma Indus suture dominant volcanic and felsic absence of Cr-Spinel main peaks at 58 Ma and 98 Ma Late Cretaceous: +4.2 to +14 Henderson et al. (2010); molasse plutonic lithics dominant age at 480–1250 Ma Paleocene–Eocene: +1 to Wu et al. (2007) deposits +14 (with few grains with –2 to –8.7) Sulaiman fold- dominant metamorphic and zircon, tourmaline, main peak at 42–47 Ma; 70 Ma; –Roddaz et al. (2011); thrust belt sedimentary lithics rutile + apatite 83 Ma; 98 Ma Zhuang et al. (2015) (9%–86%) and secondary peak at 490–960 Ma Cr-spinel Katawaz Basin dominant quartz-rich lithics – main peak at 58 Ma; 80 Ma; –Carter et al. (2010); with low-grade metamorphic 93 Ma Qayyum et al. (2001) and subordinate volcanic secondary peak at 563–836 Ma lithic North Sistan ––ranging from 24.4 to 31.0 Ma; – Bröcker et al. (2013); suture zone 38.3 to 46.4 Ma; 86.1 Ma Pang et al. (2012); to 88.7 Ma; 11 Ma in North Zarrinkoub et al. (2012) Sistan suture zone and also 107 and 113 Ma Makran dominant volcanic and ZTR + apatite main peaks at 166,5 Ma; Middle Jurassic: –13 to +2 Mohammadi (2015); accretionary sedimentary lithics ≥ 75%, 88.7 Ma; 48.9 Ma Early Cretaceous: –17 to +11 Mohammadi et al. (2016b) wedge Cr-spinel and blue minor peak at 563–868 Ma Late Cretaceous–Eocene: amphibole –6 to +14 Gangdese arc– – ranging from 40 Ma to 218 Ma Cretaceous: –4.7 to +1 and e.g., Ji et al. (2009); Wen et main peaks at 46–65 Ma; +9.2 to +15.3 al. (2008); Zhu et al. (2008) 80–103 Ma Eocene: –4.1 to +15 Karakoram ––ranging 10 Ma to 110 Ma Cretaceous: –6.5 to +5 e.g., Honegger et al. (1982); batholith main peaks at 18 Ma; 64 Ma; Jain and Singh (2008); 108 Ma Krol et al. (1996); Parrish Kohistan-Ladakh ––ranging from 29 Ma to 154 Ma Cretaceous: +6 to +17 and Hodges (1996); arc main peaks at 58 Ma and 98 Ma Eocene: –7.40 to +14 Phillips et al. (2004); Ravikant et al. (2009); Schaltegger et al. (2002); Schärer et al. (1984); Singh et al. (2007); Weinberg et al. (2000) Zahedan-Shah ––40.5–44.3 Ma (Eocene) Eocene: –7.13 to +8.54 Mohammadi et al. (2016a) Kuh plutonic belt 28.9–30.9 Ma (Oligocene) Oligocene: -3.3 to +11.65 Sanandaj-Sirjan ––35–60 Ma; 90–110 Ma; Neoproterozoic: +2.2 to –2.6 e.g., Chiu et al. (2013); metamorphic 144–157 Ma; 160–185 Ma; and –7.3 to 10.7 Fazlnia et al. (2007); zone 568 and 637 Ma with inherited Mesoproterozoic: +8 to +9 Mahmoudi et al. (2011); cores of 800–900, 2000, 2400, Archean: 0.0 Nutman et al. (2014); 3600 Shahbazi et al. (2010) Note: Dash indicates no data available.

Eocene, younger than Himalayan populations. shortening in Eocene–Oligocene time and rep- and 16. Misfits of sandstone framework, heavy

Indus suture molasse deposits contain detrital resented a high region preventing a connec- minerals, zircon U-Pb ages, and eHf(t) exclude zircons with main peaks at 58 Ma and 98 Ma and tion between the Gangdese and regions to the all of these areas as sources of Eocene–Oligo- Hf isotopic compositions that are noncompliant southwest. A connection through the Indus and cene detritus of the South Sistan Basin. There- with Sistan detrital zircon ages. Furthermore, Yarlung probably did not start before the late fore, equivalents of the Chagai-Raskoh mag- Cr-spinel as a key heavy mineral is absent in the Oligocene–Miocene (e.g., Carrapa et al., 2014; matic arc remain the most plausible source. Indus suture molasse deposits, but represents as Dai et al., 2013). much as 20% of the South Sistan Basin heavy A compilation of the main provenance indi- Regional Tectonic Implications mineral assemblage (Figs. 15 and 16; Hender- cators from north to south of the Himalayan son et al., 2010; Wu et al., 2007; Table 1). The system, including the Gangdese and Kohistan- A large quantity of detrital material in the Gangdese batholith is characterized by Creta- Ladakh magmatic arcs, the Karakoram batholith, South Sistan Basin is derived from rocks with ceous and Eocene ages, with a peak ca. 50 Ma; the Zahedan–Shah Kuh plutonic belt, the Sanan- ages and compositions comparable to rocks of the Late Cretaceous (89 Ma) main peak of Sistan daj-Sirjan metamorphic belt, and contempora- the Chagai Hills–Raskoh arc system. In this arc zircons is almost absent there (Fig. 16; Wen et neous sedimentary basins including the Kailas system, a late-Early Cretaceous–Late Cretaceous al., 2008). In addition, Hf isotopic values from Basin, the Indus suture molasse deposits, the (120–65 Ma) intraoceanic island arc collided the Gangdese are more positive than the Hf val- Sulaiman fold-thrust belt, the Katawaz Basin, with the Eurasian margin (Afghan block) in lat- ues recorded in the Sistan zircons (Fig. 15; Ji et the North Sistan Basin, and the Makran accre- est Cretaceous–Paleocene time; the collided arc al., 2009). The Tethyan Himalaya was actively tionary wedge, is given in Table 1 and Figures 15 then evolved during the Eocene to Oligocene as

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a mature Andean-type continental margin and (Folk, 1980). The Zuffa (1985) method was applied to count reworking and transport processes in the Indus River lithic fragments. Minerals >0.063 mm within polymineralic by U-Pb dating of detrital zircon grains: Global and Plan- continued as such to the present (Nicholson et al., lithic grains were counted as monomineralic grains. Results etary Change, v. 76, p. 33–55, doi:10.1016/j.gloplacha 2010; Perelló et al., 2008; Richards et al., 2012; were converted to percentages for compositional comparison .2010.11.008. Siddiqui, 2004). Extending this information to (Weltje and von Eynatten, 2004; Table S3). To display the data Andersen, T., 2002, Correction of common lead in U-Pb analy- we applied five standard complementary triangular diagrams ses that do not report 204Pb: Chemical Geology, v. 192, the South Sistan Basin, the first appearance of (QFL, QmFLt, LvhLsLm, QmPK, and QpLvLsm; see Fig. 8) p. 59–79, doi:10.1016/S0009-2541(02)00195-X. (Dickinson, 1985; Folk, 1980). Blichert-Toft, J., and Albarède, F., 1997, The Lu-Hf isotope geo- Cretaceous zircons with positive eHf(t) and detrital Cr-spinel in sandstones records accretion of chemistry of chondrites and the evolution of the mantle- crust system: Earth and Planetary Science Letters, v. 148, an intraoceanic subduction system to the Afghan Heavy Mineral Separation p. 243–258, doi:10.1016/S0012-821X(97)00040-X. Approximately 2–3 kg of fresh rock was collected for each Blichert-Toft, J., Frey, F., and Albarede, F., 1999, Hf isotope continental margin at 65–55 Ma (Siddiqui et al., sample for heavy mineral analysis. To obtain transparent heavy evidence for pelagic sediments in the source of Hawai- mineral fractions (density 2.9 g/cm3 and typically <1% of bulk 1988). The newly accreted arc became a tran- ≥ ian basalts: Science, v. 285, no. 5429, p. 879–882, doi: rock), sandstones were crushed with the SelFrag apparatus sitional continental arc during the Eocene, as 10.1126/science.285.5429.879. batch equipment using high voltage (130–150 kV) pulse power Bouilhol, P., Jagoutz, O., Hanchar, J.M., and Dudas, F.O., 2013, recorded in the detrital zircon pattern, and a technology, which liberates morphologically intact minerals. Dating the India-Eurasia collision through arc magmatic From the <2 mm sieved fraction, carbonate was dissolved mature Andean-type continental margin in the records: Earth and Planetary Science Letters, v. 366, in warm (60–70 °C) 10% acetic acid. Heavy minerals were Oligocene. This places the complete closure of p. 163–175, doi:10.1016/j.epsl.2013.01.023. pulled out in separation funnels (Mange and Maurer, 1992) Bröcker, M., Rad, G.F., Burgess, R., Theunissen, S., Paderin, I., the SSZ in the late Oligocene (25–23 Ma), more from 0.063–0.4 mm sieve fractions using bromoform (density Rodionov, N., and Salimi, Z., 2013, New age constraints 2.88 g/cm3). The bulk heavy mineral fractions were mounted recently than previously accepted (Şengör, 1990; for the geodynamic evolution of the Sistan Suture Zone, in piperine (Martens, 1932) between a glass slab and a cover. eastern Iran: Lithos, v. 170, p. 17–34, doi:10.1016 /j .lithos Tirrul et al., 1983). Identification and quantification were carried out under a .2013.02.012. petrographic microscope by applying the mid-point ribbon Burg, J.-P., 2011, The Asia-Kohistan-India collision: Review and fleet counting methods. At least 200 grains were counted CONCLUSIONS and discussion, in Brown, D., and Ryan, P.D., eds., Arc- per sample (Mange and Maurer, 1992). Results were converted continent collision: Springer-Verlag Frontiers in Earth to percentages for compositional comparison (Table S4). Sciences, p. 279–309, doi:10.1007/978-3-540-88558-0_10. Our work assessed the provenance of detrital Camp, V., and Griffis, R., 1982, Character, genesis and tec- material in Eocene to Oligocene turbiditic sand- Detrital Zircon Separation and Hafnium Isotope tonic setting of igneous rocks in the Sistan suture zone, stones of the Neh complex of the South SSZ. Ratios eastern Iran: Lithos, v. 15, p. 221–239, doi:10 .1016 /0024 Detrital zircons were extracted using standard min- -4937(82)90014-7. Results yield protolith ages from Late Creta- eral separation techniques such as dissolution of carbonate Carrapa, B., Orme, D., DeCelles, P.G., Kapp, P., Cosca, M.A., ceous to Eocene (115–50 Ma). The late-Early cement in cold hydrochloric acid and heavy liquid separation and Waldrip, R., 2014, Miocene burial and exhumation of Cretaceous εHf values range from -17 to +33 (methylene iodide, density 3.32 g/cm3). Hand-picked zircons of the India-Asia collision zone in southern Tibet: Response (t) three different sizes (fine, medium, and coarse) were mounted to slab dynamics and erosion: Geology, v. 42, p. 443-446, and Eocene εHf(t) values range between -15 and in epoxy blocks and polished to core exposition. All analyzed doi:10.1130/G35350.1. +26. The combined U-Pb ages and Hf isotope zircons were controlled and photographed with cathodolu- Carter, A., Najman, Y., Bahroudi, A., Bown, P., Garzanti, E., and data suggest that the protolith rocks belonged to minescence and backscattered electron imaging (Jacobsen Lawrence, R.D., 2010, Locating earliest records of orogen- and Wasserburg, 1980) from a split screen on a CamScan esis in western Himalaya: Evidence from Paleogene sedi- a Late Cretaceous intraoceanic island arc trans- CS44 scanning electron microscope at the ETH Zurich to ments in the Iranian Makran region and Pakistan Katawaz formed into an Eocene transitional continental determine inclusions and internal structures of grains prior basin: Geology, v. 38, p. 807–810, doi:10 .1130 /G31087 .1. Chiu, H.-Y., Chung, S.-L., Zarrinkoub, M.H., Mohammadi, S.S., arc, likely the Sistan (westward) extension of to isotopic analysis. The laser ablation–inductively coupled plasma–mass Khatib, M.M., and Iizuka, Y., 2013, Zircon U-Pb age con- the Chagha Hills–Raskoh arc in Pakistan and spectrometry (LA-ICP-MS) analyses were performed on an straints from Iran on the magmatic evolution related Afghanistan. These results do not support the Elan 6100 DRC instrument coupled to an in-house-built 193 to Neotethyan subduction and Zagros orogeny: Lithos, nm excimer laser at the ETH Zurich. Helium gas (1.1 L/min) v. 162, p. 70–87, doi:10.1016/j.lithos.2013.01.006. hypothesis that Sistan detritus was supplied from is used as the carrier gas in the ablation cell. The laser was Chu, M.-F., Chung, S.-L., Song, B., Liu, D., O’Reilly, S.Y., Pear- Himalayan sources in a paleo–Indus submarine run at a pulse rate of 10 Hz with energy of 0.5 mJ/pulse and son, N.J., Ji, J., and Wen, D.-J., 2006, Zircon U-Pb and Hf fan delta complex. Instead, the Eocene to Oli- a spot size of 30 µm. The accuracy and reproducibility of each isotope constraints on the Mesozoic tectonics and crustal analytical run were monitored by periodic measurements of evolution of southern Tibet: Geology, v. 34, p. 745–748, gocene detritus was presumably transported by the standard GJ-1, with a 207Pb/206Pb age of 608.5 ± 0.4 Ma doi:10.1130/G22725.1. rivers and subsequent turbiditic flows from the (Jackson et al., 2004). Common lead correction done after Crimes, T., and McCall, G., 1995, A diverse ichnofauna from 202 Eocene–Miocene rocks of the Makran Range (SE Iran): Afghan active margin to the South Sistan Basin. the Hg correction based on Hg is measured by ICP-MS (Andersen, 2002). The GLITTER software (Van Achterbergh Ichnos, v. 3, p. 231–258, doi:10 .1080 /10420949509386394. et al., 2001) was run to calculate isotopic ratios, ages, and Critelli, S., De Rosa, R., and Platt, J.P., 1990, Sandstone detrital modes in the Makran accretionary wedge, south- ACKNOWLEDGMENTS errors. Isoplot v.3.0 (Ludwig, 2003) generated concordia and frequency probability diagrams. Concordant ages only have west Pakistan: Implications for tectonic setting and long- We thank the Geological Survey of Iran for efficient support been considered (Table S5). distance turbidite transportation: Sedimentary Geology, during field work. We gratefully acknowledge Jonas Ruh for The hafnium isotope ratios were measured on a Nu v. 68, p. 241–260, doi:10.1016/0037-0738(90)90013-J. his help in the field and Carla Müller for nannofossil deter- Plasma multicollector-ICP-MS (Nu Instruments Ltd) attached Dai, J., Wang, C., Hourigan, J., Li, Z., and Zhuang, G., 2013, mination. We also acknowledge Frowin Pirovino for his help to a 193 nm UV ArF excimer laser at the ETH Zurich on the Exhumation history of the Gangdese batholith, south- on sandstone thin sections, Albrecht von Quadt and Markus same zircon grains as used for U-Pb dating. A laser repeti- ern Tibetan Plateau: Evidence from apatite and zircon Wälle for their support on the laser ablation–inductively cou- tion rate of 5 Hz, a spot size of 60 µm, and He transporter (U‑Th)/He thermochronology: Journal of Geology, v. 121, pled plasma–mass spectrometry, and Karsten Kunze for his gas (0.8–1.11 L/min) were applied. The energy density was p. 155–172, doi:10.1086/669250. assistance for cathodoluminescence and backscattered elec- 10–20 J cm22 and standard Mud Tank zircon was employed DeCelles, P., Gehrels, G., Quade, J., LaReau, B., and Spurlin, tron imaging. We thank Guansheng Zhuang and Yani Najman for external correction. Each ablation was preceded by a 40 s M., 2000, Tectonic implications of U-Pb zircon ages of for providing their Hf database of Himalayan rocks, Barbara background measurement and ablated zircon was measured the Himalayan orogenic belt in Nepal: Science, v. 288, Carrapa and two anonymous reviewers for their detailed for 60 s. For an accurate measurement of Hf isotope ratios no. 5465, p. 497–499, doi:10.1126/science.288.5465.497. reviews and comments on a previous manuscript, and R. in zircons, the isobaric interference of 176Yb and 176Lu on 176Hf DeCelles, P., Carrapa, B., and Gehrels, G., 2007, Detrital zir- Damian Nance for his patience and editorial work. This study was corrected by measuring 171Yb (176Yb/171Yb = 0.897145) and con U-Pb ages provide provenance and chronostrati- was funded by the Swiss National Fund (grant 2-77644-09). 175Lu (176Lu/175Lu = 0.026549), respectively. Age corrections graphic information from Eocene synorogenic deposits to calculate initial 176Hf/177Hf ratios were obtained by using a in northwestern Argentina: Geology, v. 35, p. 323–326, 176Lu decay constant of 1.867 × 10-11 yr–1. The estimate of eHf doi:10.1130/G23322A.1. APPENDIX 1. 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