Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | nities ffi 2 700 MPa) of > , and B. Dahren 1 350 (468–130) MPa, while amphi- ∼ erentiation occurred in an open upper ff , M. Sadeghian 2 2322 2321 300 MPa) and very high pressures ( ∼ , V. R. Troll 1 , H. Ghasemi 1,2 This discussion paper is/has beenPlease under refer review to for the the corresponding journal final Solid paper Earth in (SE). SE if available. Faculty of Earth Sciences, ShahroodDepartment University, Shahrood, of Iran Earth Sciences, CEMPEG, Uppsala University, Uppsala, Sweden masses of gabbro, and2003; a Khalatbari thick Jafari sequence et of al., submarine 2013). basaltic The lavas ophiolite (Shojaat is et intruded al., by widespread subvol- tions during high-level magma storage. 1 Introduction The Sabzevar ophiolitic zoneophiolite (SOZ) belt in and represents northeastwhich a Iran was remnant obducted is of in part the lateThe Cretaceous Cretaceous of ophiolite to Tethyan the ocean belt early lithosphere eastern Paleocene contains time Tethyan ultramafic (Shojaat rocks et (harzburgite, al., 2003). dunite and lherzolite), small ing system, whichin may this have rock been suite.oscillatory-zoned Barometry, a combined and key with sieve-textured process frequent plagioclasemore disequilibrium to crystals features, evolved intensify with such samples, adakite-type An-rich as implycrustal overgrowths a final magma in magma system that di developed progressively stronger compositional modifica- models, including amphibole thermobarometry, plagioclase-melt thermobarometryclinopyroxene-melt barometry. and Based on the results ofplagioclase these crystallized thermobarometric dominantly models, at pressures of boles record both low pressurescrystallization. ( The latter iscrystallization (550 supported to by 730 MPa). theno The calculated association plagioclase of pressures in amphibole forphibole with the clinopyroxene clinopyroxene fractionation most and from primitive very samples hydrous (Mg-andesites) magmas at is deep consistent crustal with levels am- of the plumb- Subduction-related adakite-type intrusivePaleocene rocks Sabzevar emplaced ophiolite into zone,in the NE composition. late Iran, Here range Cretaceous- weintrusive from investigate rocks the Mg-andesite by magma to supply applying rhyodacite system thermobarometric to mineral these subvolcanic and mineral-melt equilibrium Abstract 1 2 Received: 24 July 2014 – Accepted: 24Correspondence July to: 2014 K. – Jamshidi Published: ([email protected]) 8 August 2014 Published by Copernicus Publications on behalf of the European Geosciences Union. Magma storage and plumbing of adakite-type post-ophiolite intrusions in the Sabzevar ophiolitic zone, NE Iran K. Jamshidi Solid Earth Discuss., 6, 2321–2370,www.solid-earth-discuss.net/6/2321/2014/ 2014 doi:10.5194/sed-6-2321-2014 © Author(s) 2014. CC Attribution 3.0 License. 5 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 2.3 Ma) (Lensch ∼ conditions of amphibole and T - 10 km wide and represents a tec- P ∼ 2324 2323 200 km long and 40 Ma) to the end of the Pliocene ( ∼ ∼ erences between the post-ophiolite subvolcanic rocks of the ff C in calc-alkaline compositions (Blundy and Holland, 1990) and ◦ C to 1150 ◦ The composition and growth morphology of igneous feldspar usually reflects pro- Amphibole occurs as essential rock forming mineral in a wide variety of igneous and The detailed evolution and ascent history of the Sabzevar post-ophiolite rocks has 10 Ma focussed predominantly on the Turkish-Iranian plateau (e.g., Berberian and the southern part (Fig. 2). Fragments of host rocks, including serpentinized harzbur- sedimentary rocks are composed of marineyounger flysch-type facies are facies in of their continental lower origincentages parts, and while of contain, in volcanic someoften parts, detritus. extremely steeply These high per- dipping sedimentary(Ghasemi and rocks et are penetrated al., tectonically 2011). bythe Following imbricated, Oligocene Oligocene the volcanic alkali-olivine-basalt Eocene activity, magmatism volcanic magmatism to recommenced the and in end the volcano-sedimentary of region the and and Pliocene.canic In continued rocks the occur Sabzevar belt, in characteristically, post-ophiolite thematism subvol- north comprised and intermediate in rocks the in the south northern of the part, ophiolite while zone felsic (Fig. rocks 1) dominate and mag- 1982; Bina et al., 1986;2012) Stampfli and and Borel, Eocene 2002; volcano-sedimentary Agardregion. rocks et Since cover the al., extensive Oligocene, 2005; volcanism areas Shabanian has∼ in et been al., the intermittent (Jahangiri, Sabzevar 2007) and,Berberian, for 1981; Keskin et al., 1998; Azizi and Moinevaziri, 2009). The Oligo-Miocene Cretaceous rifting from acrocontinent narrow from but the deep Eurasian seaway, separatingof plate. the northeast The Central ophiolite dipping Iranian wasOcean) mi- subduction emplaced in (i.e. during Upper an closure)placement Cretaceous–early episode of of Paleocene the the time Sabzevar Tethyan ophiolitic (Shojaatism seaway belt from was (the et followed at by al., Sabzevar least lasting 2003).et the post-ophiolite Eocene volcan- The al., ( 1977; em- Spiespressed et in al., central 1983; and Shojaat in et northern al., Iran 2003). (Berberian This and Eocene King, volcanism 1981; is Berberian ex- et al., The Sabzevar ophiolite zone is tonically dismembered ophiolite complex,Central located along Iranian the microcontinent northernsuggest (Shojaat boundary that et of the Sabzevar the al., ophiolite 2003). was part Plate of tectonic the Tethyan reconstructions Ocean that formed during 2 Geological setting barometry. gressive changes in crystallizationtion conditions dynamics that of give an associated a meltand reliable and its record Schmincke, thermal of 2002; and crystalliza- compositional Slaby historyplagioclase and (e.g. are Troll Götze, found 2004). most Inemployed widely the the in thermobarometers of studied the Ridolfi northern rocks, andto Renzulli amphibole suite determine (2012) and of for crystallization selected intermediate amphiboles andthermobarometry rocks storage and (Putirka, conditions we for 2008) thesewere and rocks. employed Plagioclase-liquid clinopyroxene-melt in barometry order to (Putirka, complement 2008) and test the results from amphibole thermo- mental studies have synthesized amphiboleand over 400 a pressure rangeamphibole of has up therefore to considerable potential 2300tions, MPa as both an as indicator geothermometer of crystallization and2010). condi- geobarometer (Blundy and Holland, 1990; Ridolfi, on the history of the post-ophiolitefelsic intrusive suite. rocks We attempt in to the compareNorth post-ophiolite and southern aim Sabzevar to test belttwo if with sectors di exist. dominantly Finally, intermediateplagioclase we ones crystallization hope in through to the establish mineral-meltreconstruct the the equilibrium former thermobarometry plumbing system to to help these rocks. metamorphic rocks and is especially abundant in calc-alkaline igneous rocks. Experi- of this study ispost-ophiolite to subvolcanic investigate rocks. the compositional spectrum and ascent historynot been of investigated these previously andwhole we rocks present plus new major major element and data trace from element the data main on minerals to improve our knowledge canic stocks and dykes of intermediate to felsic compositions and the main purpose 5 5 25 20 10 15 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | = C and ◦ 36 ± erence after 150 MPa and ff ± ”. Major, trace ele- in a wide range of amphibole 2 O conditions were estimated from f melt and www.acmelab.com O 0.37 log units) up to 500 MPa (NNO 2 T , ± P 2326 2325 0.78 wt.%) for calc-alkaline and alkaline magmas up ± NNO values ( ∆ melt background. For calibration of all elements a set of mineral O 2 ± ers). Application of this method is limited to igneous amphibole ff C. Trace elements and REE concentrations were obtained by solution 11.5 %, H ◦ ± P C, aceous siltstone and marl are found in some intrusions as xenoliths (Fig. 3). ◦ C and 2200 MPa and ◦ ff 23.5 ± Major element analyses on selected minerals (amphibole, plagioclase and pyroxene) 247 MPa (Putirka, 2008), which is less precise than the amphibole barometer em- T barometry. This model isisting melt based in on hydrous magmatic Al systems. partitioning The SEE between for this clinopyroxene barometer and is coex- ployed. The most commonly used nominal meltscompositions are (Putirka whole et rock, groundmass al., and 2003; glass applied Putirka, as 2008) the and nominal the melt respective in whole our rocks study. were 3.4 Clinopyroxene-melt barometry This barometry model forhas clinopyroxene-melt been equilibria after applied Putirka to (2008, cross-check Eq. 32c) the result from amphibole and plagioclase-melt 3.3 Plagioclase-melt thermobarometry To test and complement the results ofmelt the thermobarometer amphibole thermobarometry, the of plagioclase- Putirkause. The (2008), standard calibrated error for± of hydrous estimation systems, (SEE) was for put this to thermobarometer is compositions) allows to estimate the( physico-chemical parameters at low uncertainties to 1130 nickel-nickel oxide bu phenocrysts and cannot be appliedmicrolites to or fluid-related quenched amphibole (hydrothermal) zones amphiboledisequilibrium in veins, conditions erupted to (Ridolfi products and that Renzulli, likely 2012). reflect variable Temperature, pressure, oxygen fugacityamphibole and compositions H using theRenzulli recent (2012), thermobarometric which is formulation able of tocrystallization estimate Ridolfi the conditions. and Their new single-crystal model (requiring only the amphibole 3.2 Amphibole thermobarometry fusion and dilute nitricignition at digestion. 1000 Loss oninductively ignition coupled plasma-mass (LOI) spectrometry isanalytical (ICP-MS) by details for weight and whole di uncertainties rocks. please For further see “ 3 Method 3.1 Analytical techniques Twenty-three fresh whole rock samplesthe from the southern northern sector sector were andalytical selected 24 for laboratory, samples major Vancouver, from and Canada.determined trace Total by element abundances ICP-emission analysis of spectrometry at AMCE following the an- a major Lithium oxides metaborate/tetraborate were Large volumes ofPleistocene detritus conglomerates originated (Fig. 3d), from whichoutcropped these indicate at that intrusive the the domes, studied Earth’s domesjad, forming surface eventually 2008). around Pliocene- the Miocene-Pliocene boundary (Salehine- gites, tu plementary clinopyroxene crystals. Representativeare compositions given of in selected Tables 2 minerals and 3. cluded an accelerating voltage of 1510 kV, s a on beam peaks current and of 5and s 10 synthetic nA on and standards counting has timeslines. of been The used. analysed All data elements setand were consists 29 of analysed on 197 using clinopyroxene, points collected K on from (alpha) amphibole, 30 212 amphibole, on 26 plagioclase plagioclase and five com- ment data for post-ophiolite subvolcanic rocks are listed in Tablewere 1. performed on Jeol JXA 8530F Hyperpobe at CEMPEG. Analytical conditions in- 5 5 25 15 20 10 10 20 25 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.05 at ± ) form phenocrysts 15 -An 5 0.08. All datapoints plotting ± 0.65). Monomineralic glomerocrysts of ≈ C (Putirka, 2008). The plagioclase compo- ◦ 2328 2327 1050 T > cients of the anorthite and albite components, Kd[An-Ab]. 0.11 at ffi ± cient of Fe and Mg between clinopyroxene and melt. The accept- ffi C and 0.27 ◦ 1050 erent components that crystallize from a nominal melt are compared with observed Dacite samples from light-grey domes and dykes show plagioclase as the volumet- Felsic rock types of broadly rhyolitic compositions crop out as dominantly white- Euhedral to subhedral biotite is present and in more evolved trachydacites and is Clinopyroxene-melt equilibrium was tested using two models. Firstly, we looked at ff Some embayments are short and close to the margin, whereas others are penetrating compositional zoning (Fig. 4e).the Amphibole medium and to biotite fine-grainedphibole phenocrysts groundmass microcrystals is are with usually apparent biotite, Fe-Ti composed and tions. oxides of and plagioclase apatite occurring and in am- smaller propor- coloured domes in thesanidine, southern and and plagioclase southeastern (typically albitein part in a of composition, fine-grained the An groundmass Sabzevar (Fig.quently belt. 4f). straight Quartz, Although edges, smaller quartz many phenocrysts large have fre- crystals display embayments and round edges. amphibole and biotite. Somegrained trachyandesite and samples rounded also crystal contains clotseuhedral up small microcrystals to but of 2 coarse- mm plagioclase, in amphibole diameter and (Fig. accessory 4d) apatite. that arerically made dominant up phenocryst of phase, which usually displays polysynthetic twinning and shaped or long prismsfine-grained hornblende, up plagioclase to and augite. 1 cm and the groundmassmoderately of enriched the in dykeamphibole Mg is do (average composed occur Mg# of occasionallyinclude in apatite, the Fe-Ti trachyandesite oxidesas samples. and euhedral Accessory rare needle-like minerals alkali phenocrystalsoxides feldspar. and Apatite (mostly as is magnetite) inclusions ubiquitous, occur in occurring as larger phenocrysts. euhedral Fe-Ti microphenocrysts and as inclusions in erals together with variablein amounts the of groundmass plagioclase, biotite (Fig.augite and 4a composition are Fe-Ti and only oxide found b). in microlites rock Clinopyroxene a is high phenocrysts a Mg-andesite of mafic samples basaltic (Fig. mostly 4c). andesitebut Notably, diopside and this lacks shows to plagioclase amphibole as and phenocryst clinopyroxene phenocrysts, phase. Amphibole phenocrysts are generally star acicular and fluidal textures and contain plagioclase and amphibole as the main min- oclastic rocks and appearcur as as grey-green dykes dome-forming also. intrusions In in thin the section, field, the andesite/trachyandesite but rocks oc- show porphyritic, 4 Results 4.1 Petrography Post-ophiolite magmatism inmediate the rocks northern ofdesite/trachyandesite andesite, part rocks trachyandesite, intrude of trachydacite into Sabzevar to the belt dacite ophiolite composition. comprises complex An- inter- and younger volcan- within this range were(1999), based further on tested the usingdi equilibrium the partitioning equilibrium of testclinopyroxene Na-Ca-Al. components presented There, and predicted in values mineral-melt Putirka between of equilibrium predicted and pairs observed require components to a satisfy close equilibrium match conditions. on the partitioningThe coe equilibrium constantT is < sensitive tonents which temperature are and nearperature should to conditions equilibrium be should with fall 0.10 a withinand given the mineral composition. Kd[An-Ab] melt envelope at appropriate the for given this pressure melt andthe tem- partition coe able range of equilibrium values for Kd(Fe-Mg) is 0.27 2008). 3.5 Equilibrium tests Putirka (2008) present an equilibrium test for plagioclase-melt thermobarometry based the respective input melt was the corresponding whole rock composition (cf. Putirka, 5 5 25 20 10 15 20 25 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 3 2 Y O, / O 2 7.9, 2 = N O, K 2 Yb) / . Because the 2 O contents of 2 to 2 FeO]) ranges from 37.5 O ratios of 1.3 to 3 and + (OH; F; Cl) 2 O contents (0.6–2.9 wt.%) 2 K 22 / indicates that the magma may O O of 20.2 (Fig. 7c and d), deple- [MgO 2 2 / 1V 8 , falling into the rhyolite field of O-saturated rhyolite melt due to N 2 2 T , but positive trends for Na V1 5 Yb) 2 MgO C / 2 × B 1 − 0 . The samples from the northern part have 2330 2329 total O (after Castillo, 2011), shows most of our samples 2 Nb ratio vs. SiO / Na contents (14.2–19.1 wt.%). K + 3 O La), but with both groups being enriched relative to their HF- 2 / Yb but low Y and Yb. The absence of significant correlations / Nb). According to these plots, the rocks are also characterized / O of 4.6 to 7.1 wt.% resulting in Na O (3.9–7 wt.%), belonging to the calc-alkaline (Fig. 5b) and metalumi- 2 2 Y ratios are observed (Fig. 6), indicating magmatic crystallization and erentiation due to enrichment in incompatible elements. Multi-element Nb; La / , MgO, CaO and Zr ff Y and La / / total contents of 55 to 64.0 wt.% and fall into the andesite, trachyandesite, trachydacite , FeO Sr and Sr 2 2 / Notably, the samples of the southern part have higher silica contents than the north- is based on the generalwater chemical formula and A halogen contents of the amphiboles are unknown, the amphibole formula 4.3 Mineral chemistry 4.3.1 Amphibole Amphibole phenocrysts are foundchyandesite as and euhedral dacite crystals samples withdesite and normal dykes mostly from zoning the as in northern acicularysed the part for or tra- major of element star-shape the compositions. study crystals Amphibole area. classification in (after Selected Leake amphiboles an- et were al., anal- 2004) tions in Nb, Ta and Ti,and enrichments high in Sr U andbetween K, major a and mildly incompatible element positive ratios tohave vs. experienced absent SiO other Eu processes anomaly, in addition(Fig. to 6). closed system fractional crystallization the TAS diagram (Fig.4.2 5a). wt.% They and have Na highthe alkali rocks classify contents as with high-Kcontents K calc-alkaline and range peraluminous from (Fig. 5b 15(Fig. and 5d). to c). Sr 21 The wt.% Al concentrationsYb and vary (0.5–1 ppm) the from contents calculated 208 similarDrummond, to to Mg# the 1990). 893 numbers ppm, range The from with observedtheir adakite-like in 25 low fractionated typical geochemical Y to REE adakites features (2.2–13 55 patterns (Defant ppm) are and with and a further mean underlined (La by ever, a few samples plotwhile near a the plot intersection of of Sr thein against adakite CaO the and high the silica arc-related adakite field fields, (Fig. 8b). ern suite and range from 68.9 to 73.6 wt.% in SiO typical arc-related calc-alkaline composition (cf. Defant and Drummond, 1990). How- 19 ppm) and Yb (0.4–2diagram ppm) (Fig. compared 8a) to most typical of arc the volcanics samples and plot in in the the Y field vs. of Sr adakite rocks as opposed to chondrite- and mantle-normalized plotscal for subduction-related these trace samples element patterns, (Fig.relative including 7a to enrichments LREEs and (e.g. in b), Ba LILE show elements SEs typi- (e.g. Ba by an overall enrichments inU LREEs and relative to Zr HREEsof depletions of adakite-type in on rock average HFSEs, (La compositionsalso and (e.g. contain absent Defant high Eu concentration and of anomaly, Drummond, Sr which 1990). (avg. are The 460 ppm) typical samples and features low concentrations of Y (5– are less than Na nous to peraluminous (Fig. 5c) series.to Mg# 75 (100 (Fig. 5d).TiO Strong negative correlations canRb be observed inassociated Harker di diagrams for 4.2 Whole rock geochemistry For the purpose offree), plotting, and all iron oxide content valuesSiO is have given been as normalized FeO and to dacite 100 fields % of (volatile the(0.4–0.7 total wt.%) alkali and vs. high silica Al diagram (TAS; Fig. 5a). They have low TiO ments in quartz isascent dissolution and in decompression superheated or andChang magma H and mixing Meinert, (e.g. Donaldson 2004).form, and White-coloured but is Henderson, sanidine often 1989; occurs altered. Intensely toowere altered not and grains selected has of for sanidine a microprobe are analysis. subhedral cloudy and turbid and deep into the core of the grains. The most suitable processes to explain deep embay- 5 5 25 20 10 15 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) 70 24 − 40 (0.28) to An A 53 K) (from 0.43 cations per + A 3 + K) + (from 1.59 to 1.63 ) vs. Si classification , C site) vs. four-fold and Fe IV + VI 2 ) and dacite (An VI ) and amphiboles from B 49 Fe − + 30 (1.36) and (Na Na) (from 0.26 to 0.46 p.f.u) and + IV (Fig. 9b). According to the plot (Mg IV / 3 + . The oscillatory zoned amphibole phe- A ). Despite some homogeneous plagioclase K) 8 − (1.77 to 0.59 p.f.u) and (Na 2332 2331 + 15 IV (andesine), respectively. Plagioclase is the volumetri- 56 Al and (Na (from 0.30 to 0.41). The cores are overgrown by a layer IV A K) to An + 36 vs. Si p.f.u (Fig. 9f), implies the dominance of edenite-type (Na, A K) ) substitution for the presented amphiboles (cf. Murphy et al., 2012). (from 1to 0.41 p.f.u), Al + values in hastingsite are less than Fe IV 2 Al after Ridolfi and Renzulli (2012), our calcic amphiboles are in equilib- Si + VI (0.17–0.47) toward the rim. The Mg-hornblende zones then grade into outer IV = A , T site) for amphiboles from all rock suites (Fig. 9e) indicates that Al prefer- IV K) IV Al + K vs. + A Although, the amphiboles are unzoned in the andesites, simple and oscillatory zon- A samples, but is rare inphenocrysts the that rhyolites (An occur inhibit the plagioclase andesites, with most complex of zoningare the of usually samples variable in unzoned types. the Plagioclase andFigure northern microlites, have 11a in part homogeneous shows turn, ex- compositions thethe compositional or feldspars spectrum minor composition of triangle. normalsieved Notably, all zoning. plagioclase textures plagioclase phenocrysts are crystals with preferentially analysed found pronounced primary in in zoning dacite in rocks plagioclaseplex) (Fig. are types: 11b dominant and and c). include Two normal types and of oscillatory (com- in length do occur in somesuite dacite comprises samples plagioclase from as the northern phenocrystsclase part. and phenocrysts The microlites. southern in The rhyolite the composition(labradorite) of andesite plagio- and and trachyandesite An rocks rangescally from dominant An phenocryst phase in the trachydacite (An trend in Fe to 0.33), while(Fig. a 10b very and c). mild increase in Mg4.3.2 is observed Plagioclase (from 3 toPlagioclase 3.14 occurs cation abundantly p.f.u) samples together as with individual phenocrysts, amphibole microphenocrysts,clase in and crystals microlites. the Although commonly plagio- northern range between subvolcanic 0.5 and 3 mm, large phenocrysts up to 7 mm of dark Mg-hornblende andcompared show to the significantly cores. lower Interval(from Al changes 3.17 in to this zone 2.62(Na are cations marked p.f.u) by decreases andrims in with increases Mg ferrian-tschermakite in composition, reflecting Al normal zoning with a decreasing in the core tocation 2.8 p.f.u) cations and p.f.u. (Na in the rim) and an increase in Al zoned amphibole phenocrysts aresmall characterized subhedral inclusions by of broad Fe-Tiphenocrysts cores oxides (not are that shown). tschermakite commonly The and host cores showcoupled of a the with progressive simple-zoned decrease rimward increase in nocrysts in in Mg the dacite that and is bright trachydacite euhedral samples zones are in illustratedized by back-scattered by alternating a images dark tschermakitic (Fig. and coreand 10a). that apatite. also This The commonly zoning cores hosts is small of inclusions character- these of minerals Fe-Ti shows oxides a rimward decrease in Mg (from 3.44 entially resides in thebetween tetrahedral (Na site, which,K together with the negative correlation ing is present in amphiboles from the trachyandesites and trachydacites. The simple- diagram (Fig. 9). Thetschermakites, amphiboles and from those the inmakite, andesite the while trachyandesite samples and amphiboles are trachydacite Mg-hastingsites fromMg-hastingsite samples can to dacites are be separated tscher- are from pargasite mostlyformula; by Al magnesio-hornblendes values of (Fig. Al 9c). of rium with calc-alkaline liquidsAl (Fig. (Al 9d). A plot of six-fold Al (Al formula unit (apfu) ofthe Ca northern and subvolcanic Nahave suite in Si the plot B between in site, 6(Leake, the 1978). (i.e. and calcic The (Ca compositions 7 amphibole oftrachydacite values field. the and amphiboles per These dacite from samples formula, amphiboles the are andesite, characteristic shown trachyandesite, in of the igneous Mg amphiboles is calculated to 23(O). Amphiboles are classified through the number of atoms per 5 5 25 15 20 10 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | C to An ◦ 10 − 50 0.5) (cf. 370 MPa ± magnesio- ∼ T - P 395 MPa (780– C. ◦ C and estimated ). Simple resorp- ∼ ◦ ) and are mantled is accompanied by 44 190 MPa (226–145), 34 − An ∼ 24 to An 0.21) (Ridolfi et al., 2010). 39 < 100 µm) often follow, and are 320 MPa (388–268) in trachy- ∼ O values known in calc-alkaline C, respectively (Fig. 12a). Mag- ∼ ◦ 2 820–700 MPa) correspond to the 9.8, respectively. Mg-hornblendes values of 3.7 to 8.2 wt.% ( ∼ − magnesiohornblende (avg. 190 MPa, melt T - O (e.g. from An P 2 pattern of extrusive rocks and glasses (cf. 10.9 (Fig. 12b). Tschermakites from crys- 11.0 to 2 An − − 0.21 that were synthesized in equilibrium with 2334 2333 ≤ ) for Mg-hastingsites in andesites range from ) for tschermakites from trachyandesites and tra- 2 2 O vs. SiO O 12.1 to f f ) similar to trachyandesitic samples ranging between 3 9.5 and C) to lower − 2 ◦ O − phenocrysts are frequently found in trachydacites and O 2 f C and from 858 to 946 ◦ ) overgrowth rims. This increase in X ) from 11 to 2 -T of the amphibole suite is given in Fig. 12c, where the sta- 47 − ) followed by several zones with markedly higher anorthite con- − O f is also present in a fraction of feldspars and consists of alterna- 39 36 melt O 2 in plagioclase implies a composition change from calcic to less calcic to An ) (Fig. 11b and d). These An-rich compositions are then usually followed 29 55 ) and applied this value to the sub-ophiolite units also (see Discussion). − 9.3 (Fig. 12b). Oxygen fugacity generally increases from high 3 46 − − and likely reflect periods of stable growth from progressively evolving melts that C), consistent with the compositional variations known for calc-alkaline magmas ◦ 8.9 (Fig. 12b). Values of log ( 39 − 23.5), while tchermakitic amphiboles from the trachyandesite and trachydacite sam- A diagram of H The oxygen fugacity of a crystallising magma is reflected in the Mg content of result- Amphiboles from andesites yield pressures of on average 556 MPa (820–349) Sieved texture plagioclase Normal zoning Oscillatory zoning 10.4 to ± This Al-value is, in turn,Ridolfi in and equilibrium with Renzalli, H 2012), which agrees with the H from experiments (Gill, 1981;Gaillard, Martel 2006). et al., 1999; Müntener et al., 2001;bility Behrens field and of experimental amphibolesamphiboles comprise is crystals outlined with by Al# amelts dotted overlapping curve. the The main experimental Ridolfi Al et al., 2010).mentally All determined studied equilibrium amphibole amphiboles samples with low-Al# fall ( within the range of the experi- of dacites show logtal ( clots have a value− of log ( hastingsite (avg. 700 MPa, 990 840 dacites are derived. Mg-hornblendes in daciteswhile yield pressure tchermakites of from crystal217). clots To reconstruct gave the an plumbing average system,(3.0 we pressures g used cm of the density of the ophiolite complex ing amphiboles and values of logto ( chydacites range from temperatures for amphiboles in the clots range between 874 and(Fig. 974 12a). The highestMg-hastingsites crystallization from the pressures basaltic ( andesite.(714–246) Average for pressure estimates tschermakites of in trachyandesites and nesian hornblendes from the dacite samples range from 836 to 873 ( ples range from 868 to 960 dacites and generally(Fig. show 11c resorbed and coresby e). more and Broad An-rich oscillatory-zoned patchy (An an cores overgrowth increase rims are in Fe usuallySchmincke, and 2002), albite Mg thus (An and being symptomatic usually of follows magma a mixing. partial4.4 dissolution event (cf. Temperature Troll and and pressure from amphiboleHigh-Mg thermobarometry hastingsites from the andesite samples yielded temperatures of 908 to 992 by steep normal zoning. Reverse zonedcharacterized outer by margins an ( overalltion increase has in taken place X atinternal some surfaces. of the internal boundaries, as marked by wavy truncated tion of thin growthet zones al., with 1996; variable L’Heureux,crease An 1997). in contents In An (cf. our (up Allegreshapes. samples, to et Oscillatory neighbouring 15 al., types mol zones 1981; appear %)rhyolite show particularly Bottinga and samples. abrupt in phenocrysts Characteristically, trachydacite, in- the have dacite(e.g. typically cores and from are euhedral in An to marked one by subhedral oftents a the (An slight increase in X with progressive growth (Bottinga etseen al., in 1996; L’Heureux, a 1997). fraction Thisdissolution of type of plagioclase surfaces zoning phenocrysts and is andAn the most microcrystals. zoned It phenocrysts lacksbecame range internal depleted in in Ca. composition from An 5 5 25 20 10 15 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , 2 247 MPa ± 0.1 ppm) and Y is in equilibrium C and = ◦ 275 and 110 MPa. 70 − ∼ 36 50 ± 435 and 190 MPa and Y vs. Y (Fig. 8a). Some ∼ / 0.5). ± Sm (73–89 ppm) and Zr (88–186 ppm) contents obtained from Mg-hastingsites / 390 and 130 MPa (Fig. 13a and b). Plagio- melt O, respectively. Tschermakitic clots suggest ∼ 2 O 600 MPa (730 to 510) are retrieved (Fig. 14c). 2336 2335 2 ) yield pressures between ∼ 10 − 0.5), while tschermakite and Mg-hornblende yield 20 ± record pressures between ) shows disequilibrium with the andesite nominal melt, 20 30 0.5) melt H − − in the binary diagrams (Fig. 6), indicating crystallization- 470 and 335 MPa (Fig. 13a and b). The lower-anorthite 1, Fig. 14a and b) satisfy equilibrium conditions with the ± 30 2 50 ∼ − records between N values between 5.5 to 9.3 wt.% ( 20 − and An melt nities include the relative enrichment of Sr, depletion of Yb and Y 30 30 O ffi − 2 50 erentiation trends. Lower contents of MREEs (e.g. Tb ff , MgO, CaO vs. SiO total To help constrain the way adakites form, we first discuss the magma composition and ence of amphibole andthat clinopyroxene simultaneously phenocrysts lacks in plagioclase as the a most phenocryst primitive phase. Mg-andesite The compositional vari- plumbing of the northern adakitesFeO suite. These illustrate negativecontrolled correlations di of TiO (3.5–8 ppm) as well asin strong more increasing evolved rocks in (e.g. Zr Davidson dacites) suggest et extensive al., fractionation 2007), ofto amphibole in dacite (e.g. agreement samples. with Prolonged its amphibole occurrence fractionation as is phenocrysts also in supported andesite by the pres- of their adakitic a and the negligible oras absent products Eu from anomalies. partial Adakitesand have melting Drummond, been of 1990), originally subducting while considered metabasalticlower later crustal source melting work materials also considered (Defant (e.g. adakites Castillo, 2012). to potentially form from The Cretaceous to Paleocene Sabzevar ophioliticing zone northward in subduction present-day of Iran formed thenalud) dur- Tethyan oceanic plate. Post-ophiolite crust subvolcanic beneath rocks the aresouthern eastern widely parts distributed Alborz in of (Bi- the this northern zonesignatures, and and such show as characteristic negative subduction-related Nb,ments. trace-elements P The and northern Ti post-ophiolite anomalies, magmaticfrom rocks coupled show with andesite a enriched broad to LILE compositional range, ele- dacite dacite, in while composition the (Fig.field southern on 5a). rocks commonly All are used these discrimination exclusively post- diagrams, rhyolite such ophiolite and as rocks Sr rhyo- fall within the adakite Fig. 12a). 5 Discussion with pressures of the deeper fraction of amphiboles in these andesites (see above; (2008, Eq. 32c), average pressuresThese of results are higher than the results from plagioclase-melt barometry, but overlap thermobarometery results. 4.6 Pressure estimate from clinopyroxene-melt barometry Following equilibrium testing betweenas clinopyroxene nominal and available melt mafic (seeclinopyroxenes whole (sample Methods), rocks pressure estimatesanalysed were andesite determined. whole The rock selected and using clinopyroxene-melt barometry after Putirka but yields equilibrium with thetively. available Plagioclases trachydacite with and dacite An plagioclase compositions, with respec- An clase in the southern rhyolitesThe (An results ofcrustal the magma plagioclase-melt storage thermobarometer (468–110 MPa), record thus overall broadly mid- overlapping with to the shallow amphibole To test the resultseter of of the Putirka amphibole (2008), thermobarometry,estimation calibrated the (SEE) for plagioclase hydrous for thermobarom- systems, the(Putirka, was plagioclase-melt applied. 2008). thermobarometer Standard The is error Kdwith of [Ab–An] the equilibrium test whole showsrecord rock that pressures composition An between ofplagioclase the (An andesites and these plagioclase-melt pairs range between 5 and4.2 to 8.3 10.3 wt.% and 5 ( corresponding to H 7 wt.% ( 4.5 Pressure estimate from Plagioclase-melt thermobarometry magmatic suites (e.g. Gill, 1981). The H 5 5 25 15 20 10 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ) 2 Y 2 / O use f ff ) and 44 , and (An P , An T O content and/or O result in disso- 2 2 erent source compared ff and melt composition (e.g. 2 NK ratios, and are thus more O accompanied by an increase / f 2 + erentiated reservoir, crystals near O, ). 2 ff 29 H p An , and Fe P ∼ , A T K) 2338 2337 + , (Na 4.6–7 wt.%), with low A IV = O 2 400 ppm). According to the available geochemical data, the southern Yb ratios but low Y (2.2–13 ppm) and Yb (0.5–1 ppm) contents, resem- > / . This pattern can be explained by gradual cooling during crystallization (e.g. Mg Y and La The rhyolite/rhyodacite domes in the southern part of the Sabzevar zone have high Oscillatory and especially complex zoning in plagioclase is often marked by resorp- The core to rim variations in the simple-zoned amphibole phenocrysts shows an / stead there is a large compositional gap. A direct co-evolution of northern intermediate post-ophiolite adakite rocks might have beento derived the from northern a adakite di rocksNotably, however, which, oceanic, slab-derived however, awaits adakites to are generally bethe metaluminous, tested whereas southern by adakite isotopic methods. rocksfrom are partial peraluminous. melting Compared of tosilica subducted the and oceanic adakite potassium-rich crust, rocks (K the derived akin southern adakite to domes adakites are ofis high lower-crustal no derivation significant correlation (e.g.between between Wang the southern major et high-silica and al., samples incompatible 2012) and element the (Fig. northern ratios 5c). intermediate vs. There rocks, SiO but in- Sr bling typical adakites as defined by Defanttents and (209–377.5 Drummond ppm) (1990). for However, 13 the Sr ofical con- 25 adakites rhyolite samples ( are not as high as known from typ- show An-rich overgrowths rims andand embayments more in mafic quartz magmathe (when intrudes mixing present). a When interface colder, are hot moreDonaldson re-melted di and and Henderson, produce 1988; sievemately Tepley textures causes et and more al., embayments anorthitic 2001; (e.g. plagioclasefragments Andrews to (e.g. et grow Troll onto al., et e.g. 2008),plagioclase the al., but remaining cores 2004). ulti- plagioclase in This dacites interpretationMg that and is are Fe supported overgrown contents by by compared rims to sieved their textures with core elevated ( X then likely reflect crystallizationperiods under of stable magma time chambersive (e.g. conditions zones Foley with over et longer markedly increaseddacites al., An and 2013). content trachydacites However, in (up the oscillatory-zoned tobatches 15 plagioclase presence of mol in %) more of the likely mafic several reflects melts, magma succes- in mixing and line incoming with sieve-textured plagioclase phenocrysts that cores of the simple-zoned amphibole and oscillatory-zoned plagioclase phenocrysts clase composition (Nelson and Montana, 1992), which implies that the broad di nor local disequilibrium or small-scaleKolisnik, pressure 1990), and the temperature changes occurrence (Pearce ofsuch and disequilibrium as phenocryst oscillatory composition zoned andcannot amphibole textures be and explained plagioclase by and simple closed sieved textured system fractionation plagioclase alone. tion surfaces presented by roundedis or attributed wavy to truncated large-scale changes interfacesmelt in (e.g. composition temperature, Fig. and pressure, 11b) melt-H is which frequentlyPressure associated changes with that magma exceed recharge several Pascal or are mixing already events. capable of changing plagio- Humphreys et al., 2006) wherein composition response of to the changing amphiboleHolland melt has and likely composition been Blundy, controlled 1994). modified by Forlution plagioclase example, crystallization and slight (cf. crystallization increases innormal of melt-H zoned An-rich plagioclases compositions with (Housh small-amplitude variation and are Luhr, probably 1991). a Although result of mi- (Humphreys et al., 2009),2000; disrupted Chiaradia cumulates et or al.,shows crystal that 2011), mush the or zones mineral xenoliths (e.g. compositionsof (Chiaradia and Seeman, the the et crystal crystallization al., clots conditionsthat 2009). overlap ( the with Our clots the investigation in phenocryst the assemblage present of system are the associated host-rock, withoverall implying cooler rimward wall-rock crystallisation. decreasein in X Al Rooney et al.,ratios 2010) and and decrease the intense Ying concentrations fractionation compositions in of the to resulting that amphibole melt ofbole (Foley will typical have et been adakite al., increase suggested 2013), magmas. to the driv- Crystal1979), represent clots Sr the clusters products composed of of phenocrysts of amphibole (Garcia amphi- breakdown and (Stewart, Jacobson, 1975), cooler wall-rock material ations of the amphibole reflect changes in 5 5 25 20 10 15 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ), in 30 − 53 ects like crustal ff 4.5 ppm), significantly ≈ 550 to 700 MPa for clinopy- ∼ 3 ppm, Ni < 700 MPa). In contrast, the other am- ∼ 300 MPa). The absence of plagioclase in ∼ 2340 2339 er two distinct sets of pressures and temperatures, ff 5.5 wt.% in the magma source when hornblende and clinopy- ∼ er from typical subduction-related or delamination derived-adakites, ff 350 MPa; Fig. 15). Amphibole formed at both levels, i.e. at pressures of ∼ 750 and According to Chaussard and Amelung (2014), arcs with young and thin, ideally sed- The much more abundant medium-anorthite plagioclase phenocrysts (An The southern rhyolite samples are peraluminous and have low MgO (0.1–0.7 wt.%) 45 km depth. Therefore, the Mg-hastingsites in the northern part (from Mg-andesite) ∼ trol on the depths of magma storage, the shallow reservoir defined for our rock suites to evolved magmas (e.g.crustal trachydacite) evolution in for thesieve shallower the textured levels samples cores and with in document anmafic magma a question. oscillatory recharge lively zoned and Plagioclase subsequent overgrowth mixing phenocrysts providetrends processes, evidence suggest while that for crystal mineral compositional hotter, fractionation display also. imentary crusts are morebelow probable the to surface) develop than shallow arcs magma withheterogeneities reservoirs old such and (e.g. thick as 1–3 crusts. km fractures Although local or e sediment layering likely exert an additional con- equilibrium with a trachyandesite andupper trachydacite crust compositions, (equal in to turn, 300 formedage MPa in region pressure the in indicated average), bylization in amphibole agreement of with barometry amphibole an (Figs. from upper 15 stor- parental and magma 16b). in Fractional the crystal- mid- to lower crust thus likely led is composed of plagioclaseAn with plagioclases anorthite in the percent matrixsource up is with to also high consistent 70 water %. with content,bility The the based (e.g., inference presence on Sisson of of experimental and a evidencedyke high Grove, deeper and 1993; was magma plagioclase Ramos likely sta- et derivedA al., from 2005). a significant Therefore, mid-crustal mid- the water-richclinopyroxene-melt Mg-andesite to mafic barometry lower magma that crustal (Fig. showsroxenes 16a pressures magma from and of Mg-andesite. storage b). region is also supported by our stage of crystallization at athe shallower Mg-andesite level ( might indicatethe high plagioclase contents is of unstable waterwater under in may high the have water magma been pressure sourceroxene because (Wang formed et as al., phenocrysts, likely 2012). too Dissolved hydrous for plagioclase. However, the matrix phiboles (tschermakites and Mg-hornblendes) and plagioclases formed during a later ∼ record a mid- to lower crustal pressure (avg. which indicates two separate( levels of major crystallization800 to and 700 thus and 450 magmasure to storage 350 range MPa, while of the majority 450the of Sabzevar to plagioclase ophiolitic crystallized 300 zone, MPa. in however,boundary a Little Motaghi pres- beneath et is northeast al. known Iran (2012)depth and about imaged Central from structure the Iran 35 crust-mantle of shows kmmodel a the under and strong crust that Central variations of beneath of Iran Dehghani Moho et to al. 55 (1983), km we beneath assume the the Moho NE in the Iran. study Following region this at crust to form the distinct adakite melts of the5.1 southern Sabzevar region. The magma plumbing system Our amphibole, plagioclase-melt thermobarometerytry on and the clinopyroxene-melt northern barome- adakite rocks o very low abundances oflower compatible than elements those (Cr of thelower subduction-related crust. adakite rocks, We and therefore mayderived point favour from to a partial a melting crustal thickened ofWang origin the et for thickened al., crust the 2012). in southernlower the The crust region suite southern or (cf. that suite by Annen intense et probably maypropose assimilation al., have that of 2006; been partial ongoing produced melts subduction bymaterials, in activity melting which the eventually caused mid- of led to underplating mafic to upper partial and crust melting accretion and of of we this thickened mafic heterogeneous lower not derived from the northerntion alone. intermediate melts through simple fractional crystalliza- and Mg# that di but are comparable to those of lower crustal-derivation (Fig. 5d). The samples contain magmas and southern rhyolites remains possible, but the southern rhyolite domes are 5 5 25 20 10 15 25 20 10 15 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | (820– P of Cen- 0.5), consistent ff ± 0.21) and are found 23.5) and < ± C ◦ ) show pressures of crystal- 15 − 8 (992–836 O-magma was an important process T 2 values of 4.2 to 10.3 wt.% ( 2342 2341 melt O 2 nities, but while the northern suite is calc-alkaline in ffi erentiation and disequilibrium features such as complex conditions due to magmatic replenishments. ff 700–900 MPa) that is in line with results from pyroxene-melt 2 O ∼ f We are most grateful to the sta 6 km) lies somewhat deeper than the top 3 km of the crust, which likely ∼ region for the southernseems sector that also. the According southern to peraluminous,been produced silica-rich geochemical by and partial characteristics, high-K melting it of adakitecrust crustal rocks material, in have possibly from response thickened lower tofrom extensive prolonged assimilation underplating of mid- and to repeated upper crustal magmatic materials. activity or in producing the diversesector. range of post-ophiolite rocks observedOur in textural the study northern documentslution that of mafic magmatic magmazoning di recharge and was sieved textures driving in thewith plagioclase, embayed evo- high quartz Mg# and zoned inand amphibole outer variably high margin and suggests thatSelected conditions plagioclases from changed southern for rhyolites (An lization hotter between 273 to 110 MPa, implying a shallow upper crustal magma storage dacite, dacite compositions werebelt, intruded. post-ophiolite In domes the of rhyolite/rhyodacite southernon composition the part are whole exposed. of rock Based geochemical the features,rocks the Sabzevar have northern adakite-like and southern a nature, post-ophiolite the southern suite is peraluminous. All selected amphiboles from northern samplesto are be low-Al# in ( equilibrium withwith high H values assumed for “wet” primitive calc-alkaline magmaFor suites. the northern samples, the obtained barometry. The other amphibolespressure show of a 300 shallow MPa, magma whichresults. storage is, level in equal turn, to supported by plagioclase-meltThe barometry presence of amphibole andMg-andesite and clinopyroxene without the existence plagioclase of phenocrystthat amphibole in clots fractionation in of trachyandesites amphibole emphasises from high H In the northernophiolite part subvolcanic of domes the and Sabzevar dykes ophiolitic of zone Mg-andesite, (NE trachyandesite, Iran), trachy- numerous post- 145 MPa) ranges, basedmagma storage on regions or amphibole levels: Mg-hastingsitecrustal thermobarometery, in andesite pressures record records ( mid- two to lower distinct constraints from collisional and earlier deformation, Int. J. 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D.: Thermometers and barometers for volcanic systems, in: Minerals, Inclusions Petford, N. and Atherton, M.: Na-rich partial melts from newly underplated basaltic crust: the 5 5 30 25 20 15 10 30 25 20 15 10 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 2350 2349 Major and trace element contents of representative post- ophiolite subvolcanic sam- 0.68 0.58 0.52 0.48 0.53 0.71 0.56 0.70 0.64 0.66 0.44 0.59 0.43 0.50 0.45 0.48 2.87 3.37 4.53 2.57 1.94 1.97 4.06 4.55 4.03 1.85 2.07 2.70 1.49 3.12 2.28 2.68 0.13 0.11 0.19 0.11 0.06 0.07 0.16 0.11 0.15 0.18 0.10 0.10 0.07 0.18 0.15 0.11 55.01 57.35 57.42 58.28 58.29 58.74 58.74 55.53 56.86 58.81 58.97 59.49 59.28 60.10 60.41 62.56 17.25 14.25 18.06 17.08 15.03 16.70 18.59 18.24 18.22 16.75 17.27 15.20 15.59 19.07 17.82 17.74 3 3 5 O 5.27 5.26 3.91 5.42 4.80 5.47 4.06 6.05 6.68 4.15 4.13 6.97 4.38 3.98 4.93 4.39 2 2 O O 2 2 OO 1.15 2.95 1.28 1.74 2.50 1.75 0.59 1.23 1.10 1.25 0.63 1.02 1.59 1.73 1.87 0.72 2 taceous adakite-like porphyries andorogen, associated southern basaltic China, J. andesites Asian in Earth the Sci., eastern 61, 243–256, Jiangnan 2012. area, Anhui Province (easterntion, China): Lithos, implications 89, for 424–446, geodynamics 2006. and Cu-Au mineraliza- 2 2 MnOMgOCaO 0.14Na 4.23 0.13 5.21 6.03 0.13 5.38 3.91 0.15 7.06 3.25 0.18 3.96 2.83 0.21 3.51 3.82 0.12 1.50 2.61 0.11 6.44 4.98 0.11 4.31 4.38 0.24 4.40 2.76 0.16 5.25 1.86 0.13 5.63 3.74 0.17 3.08 4.56 0.04 4.59 2.06 0.06 5.21 4.62 0.09 4.12 3.06 5.41 K P L.O.I.SumBaCo 1.8 99.87Cs 99.85Ga 0.5 122 101.5Hf 44.3 2.10 99.89Nb 99.93Rb 96 54.3 16.82 0.1 2.1 101.43Sr 12.69 357.7 21.90Ta 0.1 1.8 99.89 17.40 4.2Th 35.6 143 101.63 5 1.62U 0.60 16.8 101.33 28.6 4 288V 14.02 390 3.5 99.89 2.00 0.5Zr 0.2 12.4 5 30.5 99.93 16.41Y 470 3.30 0.94 0.5 64 99.90 19.80 1.4 13.10 17.70La 0.3 2.00 99.93 130.1 0.2 1.22 780.6Ce 2.70 0.6 12.7 24.80 176 16.40 101.35Pr 135.7 0.10 1.4 350 101.91 0.1 1.49 81 39.1 21.00 17.50 5Nd 2.10 2.50 167 101.41 149.7 17 16.72 0.3Sm 208.00 403 0.40 3.3 46.7 0.80 2.20 18.5 9.13 66 16.85 2.6 0.3Eu 238 5 11.31 27.4 111 0.4 14.67Gd 14 1.00 4.7 69.20 465 1.4 0.1 2.10 9.20 2.8 153 1.6 15.82Tb 23.40 6.2 18.9 11.70 10.90 366.1 1.9 76 22.60Dy 0.10 1.7 0.5 0.6 2.20 16.30 87 102 9.97 44.2 8 2.1Ho 7.5 0.8 463.9 1.2 10.20 3.7 14.03 14 2.89 15.80 2.3 1.6Er 2.7 109 2.94 0.20 270 12.70 80 8.70 2.70 208.6 0.6 2.7 17.6Yb 14.18 0.8 0.4 1.30 1.18 15.90 134.00 206.0 2.60 10 0.2 2.8Lu 15.60 1.4 0.10 2.3 6 124 476 17.20 1.70 207.00 0.40 3.70 2.41 3.1 0.79 0.6 6 0.4 1.10 381.0 13.50 170.00 1.7 72.60 0.2 2.16 13.10 1.9 407 0.20 2.8 1.11 1.5 11 1.90 0.30 3.10 5.8 130.3 5.7 0.7 0.5 7.2 0.38 0.90 1.3 64.60 117 13.00 1.7 0.6 138 1.7 14.60 0.5 2.06 2.70 0.2 1.7 18.36 1.9 0.40 2.40 7.50 66.60 7.7 0.5 0.37 0.3 2.2 8 1.6 17.30 87 11.46 7.4 783 0.50 1.7 0.3 1.5 1.7 2.90 22.40 0.3 1.14 132 2.31 0.8 5.80 17.10 11.1 0.4 10.70 0.3 470.0 0.5 1.10 119 0.6 0.60 31.80 5 0.2 1.5 2.30 2.40 0.18 1.6 1.92 0.1 5.60 731.7 87 1 0.3 9.60 0.8 0.9 14 16 10.10 0.72 82 0.2 0.20 0.5 507.1 2.70 0.1 2.81 1.96 0.3 1.7 7.8 5 21.40 93 70.00 0.9 9.30 1.2 0.8 0.77 14 0.3 0.45 0.30 2.60 0.1 22.20 3.12 2.3 0.3 2.62 76.00 110 8.3 1.50 5 5 0.80 0.7 0.50 0.55 0.7 19 110.60 15.80 0.40 86.00 1.9 3.02 1.6 0.50 3.21 0.1 103.30 3.00 4.3 4.10 0.6 0.61 1.50 0.52 1.54 7 0.10 1.7 85.70 2.1 8 1.9 1.20 2.80 0.24 0.80 7.3 4.80 0.6 1.76 0.57 0.4 1.67 7.1 14.50 2.2 0.40 2.5 0.29 2 2 8.80 2.40 0.8 1.84 0.5 0.3 1.73 8.70 1.5 7 1.9 0.28 11.90 2.4 2.70 0.4 16.80 1.2 0.3 0.5 1.3 10.90 2.50 2.6 0.2 6.10 1.1 2.66 0.79 0.9 0.7 10.60 0.3 0.9 2.10 1.1 0.1 10.30 2.67 2.25 0.59 1.9 0.2 0.43 2.50 2 2.54 0.3 1.97 0.72 0.43 0.6 0.30 0.6 1.63 0.1 2.80 1.35 0.29 0.49 1.35 2.88 0.23 0.88 0.54 0.84 0.14 1.82 1.67 0.29 SamplesSiO N-1TiO N-2 N-3 N-4 N-5 N-6 N-7 N-8 N-9 N-10 N-11 N-12 N-13 N-14 N-15 N-16 Al FeOFe 4.30 3.37 2.44 2.57 1.94 1.97 2.19 3.03 2.69 2.78 3.11 2.70 2.24 1.68 1.52 1.78 Table 1. ples of NE Iran. Wang, X. L., Shu, X. J., Xu, X., Tang, M., and Gaschnig, R.: Petrogenesis of the early Cre- 5 Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.1 < 5 1 < 5 < 5 < 5 < 5 46.40 50.0 53.8 49.0 59 0.5 1.10 1.20 1.30 0.50 1.3 < < 5 < 5 < 0.05 0.07 0.16 0.12 0.11 0.11 0.2 5 9.00 < < 5 0.5 0.50 1.00 < < 5 5.00 2351 2352 < 5 < 0.1 0.2 0.2 0.1 0.14 0.17 0.14 0.06 0.14 0.18 0.14 0.19 0.21 0.2 < 0.66 0.50 0.40 0.44 0.42 0.39 0.12 0.18 0.24 0.13 0.14 0.18 0.16 0.16 0.31 0.17 0.05 0.08 0.07 0.05 0.05 0.06 0.03 0.03 0.06 0.09 0.03 0.07 0.06 0.04 0.08 0.10 0.02 0.03 0.04 0.02 17.64 17.53 17.62 16.88 16.94 17.23 17.52 17.55 0.03 16.63 16.34 15.24 15.53 14.90 16.45 0.32 0.34 0.38 0.34 0.28 0.37 0.35 0.36 15.19 71.39 71.17 71.59 72.30 72.59 73.22 72.09 72.30 72.32 72.46 72.54 72.64 72.92 73.14 73.62 1.62 1.55 1.53 1.63 0.81 2.70 1.25 0.25 0.30 0.51 0.28 0.41 0.36 0.44 0.24 0.49 0.48 0.42 0.32 0.41 0.15 0.470.06 0.31 0.08 0.02 0.09 0.04 0.22 0.10 0.13 0.13 0.04 0.06 0.07 0.03 0.07 0.05 0.08 0.04 0.07 0.03 0.08 0.03 0.06 0.06 0.06 0.05 Continued. Continued. 60.07 62.3117.13 64.09 15.51 62.78 17.04 68.61 18.31 63.60 18.82 63.71 17.29 69.72 16.78 70.23 20.64 70.28 20.24 70.40 18.73 70.72 19.81 70.78 18.67 70.95 16.60 71.27 70.78 18.2 17.14 15.44 3 3 5 O 5.27 5.50 5.80 5.18 5.43 5.10 0.03 0.05 0.05 0.02 0.02 0.05 0.01 0.01 5.35 2 2 O O 2 3 2 O 3.50 2.76 2.91 2.56 3.47 3.75 0.06 0.04 0.06 0.03 0.01 0.06 0.01 0.01 3.33 O 3 2 5 2 2 O 4.58 4.19 4.69 5.27 6.51 4.51 4.35 4.57 5.38 5.33 5.37 5.73 4.85 5.26 6.32 5.13 2 2 O O 2 MnOMgOCaONa 0.15K 0.53 0.05 0.97 0.26 0.09 1.85 0.20 0.09 0.37 0.25 0.04 1.26 0.21 0.08 0.42 0.13 1.52 1.19 5.12 0.40 3.48 6.50 0.26 3.10 7.07 0.51 2.65 5.57 0.80 4.21 5.27 0.60 3.55 6.22 1.34 3.17 5.58 1.63 2.36 5.17 0.05 2.32 0.15 0.92 FeOFe 0.66 0.41 0.33P 0.36L.O.I.Total 0.34BaBe 1.40 0.39 101.42Cs 99.97Ga 0.4 0.32 99.96 558.9Hf 99.98 1.4Nb 2.00 0.34 416 99.98Rb 1.30 101.53 17.40 38.6 0.9Sr 541 0.38 101.63Ta 17.2 31.7 0.4 3.20 101.50 471Th 0.34 17.66 9.40 101.61 1 14.3 70.90 0.66U 0.9 17.67 101.52 479 338.8 0.28V 34.9 16.22 49.3 0.96 101.42 0.80 5 493.8 0.6 0.80 101.55 16.90 60.4 790 1.09 0.37 3.00 4.80 0.90 101.41 507.5 2.3 12 18.20 52.7 0.6 1.18 350 101.45 2.60 0.35 1.00 466.5 0.70 99.97 18.40 68.2 10.0 3.20 1 221 2.10 445.5 0.7 7 0.36 1 2.00 16.90 83.10 0.60 362 2.50 3.1 510.1 2.00 0.25 7 18.10 1.5 72.70 0.7 1.00 365.7 5 1.00 502.8 0.70 2.7 16.80 67.80 1.90 1.3 475.5 0.6 3.00 487.8 1 9.30 1.50 17.20 52.40 0.50 0.8 1.40 537.7 310.8 1.3 0.70 2.00 18.30 92.10 7.20 0.60 1 1.30 377.5 1.70 2.10 1.90 19.80 71.30 304 0.60 2.00 6.40 0.80 459.9 2.00 1.20 17.5 65.90 2.10 508 2 1.40 0.50 1.00 246.7 6.70 0.70 46.00 1.20 1.00 1.90 644.3 1.70 0.40 1.00 47.50 9.30 0.3 1.20 0.10 283.2 1.90 42.2 1.10 74.5 0.80 314.10 7.10 1.70 1.00 1.70 2.40 523 0.70 6.30 1.01 2.2 2.10 2.00 10.60 0.50 1.20 10.60 1.50 1.00 0.40 1.90 1.00 9 0.30 1.70 0.9 1.7 1.7 SamplesSiO S-33TiO S-34Al S-35 S-36 S-37 S-38 S-39 S-40 S-41 S-42 S-43 S-44 S-45 S-46 S-47 ZrYLaCePr 74.0Nd 13.1Sm 15.6 67Eu 30.8Gd 4.3 3 3.72 9.12 52Tb 13.4 20.09 2.50Dy 9.6 17.59 7 45 1Ho 3.7 0.42 0.6 8.9 4.07 2.22 2.2 8.4 41 0.2 0.37 7 1.4 1.8 9.90 0.5 2.15 39.50 7.2 0.4 0.37 2 1.3 5.10 10.0 1.2 0.3 5 41.1 1.9 0.3 0.1 0.5 0.3 5.10 7.10 1.5 3.60 43.9 1 5.00 0.2 0.2 1.19 1.00 4.40 1.40 0.7 31.60 5.60 1.1 4.70 0.24 0.2 1.19 0.90 1.00 9.00 0.94 39.4 4.70 0.7 3.60 0.24 0.2 0.91 0.80 4.60 7.90 0.87 41.9 2.20 0.72 0.70 0.27 0.09 43.70 0.17 0.20 4.10 6.90 0.78 3.40 0.85 4.10 0.13 24.80 0.14 1.08 0.80 3.40 4.70 0.28 6.40 24.70 0.71 3.30 0.24 0.12 0.98 1.00 3.00 5.30 0.83 4.30 42 0.36 3.60 0.23 9.53 0.84 0.70 2.90 1.04 4.80 0.63 2.50 0.26 0.61 1.00 4.8 0.64 4.90 0.96 2.50 0.30 0.63 1.00 1.23 0.68 5 4.6 0.32 1.2 0.9 1.20 0.89 0.2 0.7 1.03 0.8 ErYbLu 1.07 1.06 0.17 0.1 0.1 0.1 0.4 0.4 0.1 0.7 0.6 0.1 0.4 0.5 0.1 0.17 0.11 0.01 0.41 0.40 0.06 0.33 0.33 0.05 0.13 0.05 0.01 0.14 0.10 0.01 0.45 0.46 0.07 0.30 0.32 0.05 0.19 0.08 0.01 0.21 0.11 0.01 0.3 0.3 0.1 2 OO 1.54 1.35 2.13 2.05 2.24 0.77 1.11 3.57 3.62 2.90 3.48 3.35 1.92 2.67 3.46 2.62 2 2 2 MnOMgOCaO 0.22Na 2.17 0.12 4.38 2.96 0.20 4.26 1.17 0.05 3.31 2.45 0.08 3.62 0.75 0.08 0.87 2.92 0.15 5.25 2.10 0.06 4.59 0.10 0.04 1.25 0.18 0.04 0.46 0.25 0.04 1.97 0.16 0.03 0.42 0.24 0.06 0.81 0.22 0.04 2.68 0.23 0.05 1.81 0.43 0.05 0.35 0.25 1.75 Samples N-17SiO TiO N-18 N-19FeOFe N-20 N-21 2.43 N-22 2.33 N-23K 1.53 S-24 1.63 S-25 0.81 S-26 1.80 S-27 1.88 S-28 0.25 S-29 0.30 S-30 0.51 S-31 0.28 S-32 0.41 0.36 0.44 0.42 0.40 Al P L.O.I.TotalBaCo 2.6 99.94Cs 99.98 2.4 99.95 272 101.43 22.2 1.9 101.32 181 49.5 0.4 101.4 3.10 300 99.93 26.6 0.4 101.50 445.6 1.60 101.53 9.30 463.9 1.90 101.41 1 132.5 101.41 1.20 1.8 101.44 13.60 0.90 323 101.43 31.8 1.10 101.34 518.0 0.80 100.62 2.00 545.1 0.20 0.70 99.98 481.0 2.00 0.7 0.80 559.6 2.00 1.10 539.2 1.00 318.5 1.00 413.4 2.00 3.50 424.3 1.00 1.20 408 1.00 0.80 1.00 1.4 36.9 GaHfNbRb 15.97Sr 16.28 2.69Ta 15.36Th 1.95 16.80 9U 9.3 0.58V 17.70 550 11.6Zr 15.80 0.6 8 3.20 283 42.4 15.71 3.6 0.4 358 38.70 0.9 15 2.70 2.60 1.4 64 848.5 43.10 0.9 2.80 160 0.5 5.80 1.80 4.7 673.5 10.5 0.40 88 0.9 92 7.70 0.80 10.9 3.60 1 400 18.70 2.60 0.60 186 31 1.80 670 6.80 3.80 16.10 124.30 1.20 0.10 58.00 17.40 70.10 0.70 16.40 90.10 5 3.70 1.20 19.00 0.5 88.00 17.20 73.60 16.00 90.00 1.1 337.80 0.40 2.10 5.00 17.80 58.00 344.50 71 1.90 0.60 68 894.50 0.2 1.90 4.10 16.50 68.30 335.10 17.98 811.00 2.10 65.50 0.30 1.80 1.60 2.00 512.2 0.40 35.70 2.40 0.30 1.00 1.70 1.90 810.6 52.70 0.30 2.00 0.30 1.10 208.2 1.50 5.20 65.30 0.96 0.30 774 0.50 1.00 1.50 5.40 60 0.40 0.70 6.00 1.10 5.00 0.6 0.70 7.00 0.70 5.20 0.80 7.00 1.10 5 0.9 8.00 1.30 0.8 6 YLaCePrNd 12.6 12Sm 26.61Eu 11.37 4.9Gd 10 35.1 10.9Tb 3 15.9 1.8 26.40 15 6.2 13.00 1.7 0.7 31.50 1.7 13.6 1.9 9.20 15.40 16.30 0.6 0.3 11.10 6.90 12.27 4 2.4 1.7 9.20 12.90 0.6 17.00 0.3 6.1 3.80 3.04 2.10 1.7 10.10 0.61 0.4 6.30 5.50 3.60 1.90 5 1.59 5.9 0.55 2.34 0.27 2.50 38.40 5.70 5.10 1.59 0.93 0.69 40.50 1.4 0.26 1.5 2.83 3.40 5.90 1.21 61.40 0.4 0.48 7.50 3.50 0.8 5.50 4.70 38.80 1.14 0.80 10.10 0.1 4.30 0.26 2.70 4.60 2.90 1.29 1.00 9.20 1.02 4.20 0.25 2.50 6.80 2.70 2.70 10.20 0.80 0.96 5.10 0.24 3.40 4.50 3.20 2.20 0.63 1.00 0.61 7.05 0.50 0.29 2.40 2.70 3.20 0.59 0.14 0.97 0.40 0.39 3.3 2.10 0.82 0.16 3 0.08 0.60 0.38 3.3 0.53 0.18 0.07 0.40 0.50 0.9 0.16 0.09 0.5 0.38 0.2 0.08 0.5 DyHoErYbLu 1.4 0.4 1.6 1 0.4 1.1 1.7 0.2 0.4 0.8 1 1.46 0.1 0.29 0.7 0.9 1.39 0.1 0.26 0.77 2.74 0.86 0.14 0.59 0.78 0.7 0.78 0.13 0.1 1.73 1.70 0.18 0.30 0.96 0.4 0.4 0.17 0.1 0.77 0.52 0.18 0.10 0.47 0.54 0.43 0.16 0.16 0.38 0.91 0.25 0.10 0.39 0.26 0.08 0.41 0.16 0.39 0.42 0.07 0.17 0.21 0.45 0.03 0.09 0.18 0.22 0.37 0.03 0.08 0.22 0.27 0.5 0.03 0.1 0.19 0.20 0.03 0.1 0.2 0.1 Table 1. Table 1. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 0.8 6= 0.8 Mg 6= Mg 47 An 25 An 44 2354 2353 An 55 An Plagioclase Plagioclase 0 0 0 0 0 0 0.25 0 0.054 0 0.02 0.02 1.44 0.32 Amphibole Amphibole Amphibole 0.03 0.12 0.01 0.01 0.07 0.04 0.02 3.55 3.12 1.24 1.62 1.66 1.03 1.45 29 12.77 12.58 13.43 11.16 11.52 8.79 11.11 41.03 40.71 42.6 45.31 46.09 47.73 44.98 An 63.5823.72 54.97 60.38 28.27 67.11 25.64 58.68 22.22 27.07 48.94 4.91 52.7 2 3 3 O 2.45 2.61 2.41 2.33 2.31 1.68 2.3 2 2 O O 2 O 0.96 0.99 0.30 0.12 0.2 0.19 0.18 2 2 3 Al 2 2 1.7 1.6 1.6 1.2 1.6 2 3 O 7.34 5.1 5.64 6.59 5.69 0.42 0.43 2 2 O FeOMnOMgO 10.11CaO 0.06 9.89Na 14.53K 14.95 11.99 15Cr 11.36 0 12.05 11.87 15.17 10.58 0.24 16.65 10.71 9.15 11.04 0 14.77 12.25 0.23 14.02 11.19 13.06 11.55 0.32 0.25 No.position CoreSiO N-1TiO RimAl N-1 Core N-11 Rim N-11 Core Bright zone N-4 Rim Total N-4Mg N-4 97.47IV 97.02 97.18 98.30 3.2 98.95 3.3 3.2 98.00 98.93 2.5 3.5 3.1 3 Mineral Unzoned- Simple-zoned Oscillatory-zoned O 2 O 0.36 0.14 0.26 0.46 0.23 0 0.01 2 Representative compositions of amphiboles from post-ophiolite rocks in Sabzevar 2 Representative compositions of plagioclases and clinopyroxenes from post-ophiolite 2 K Cr Total 100.72 100.11 100.22 100.67 101.66 99.71 100.00 MineralNo.Position Oscillatory-zone Core, N-17 innerSiO zone,TiO SievedAl texture Rim,FeO N-17 Core,MnO N-17MgO CPx Rim,CaO 0.08 N-18Na Core, CPx 0.02 0 N-18 5.61 0.22 Rim, N-1 0.17 0.03 11.32 0 0.12 0.03 8.09 N-1 0.41 0.00 0 4.09 0.04 9.54 7.41 0 0.02 22.91 6.06 13.67 0 21.5 16.52 0.21 Table 3. rocks in Sabzevar zone. Table 2. zone. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Simplified (b) . 1 − Presence of star- (d) Ophiolite complex Post-ophiolite dome photographs of southern post- Pliocene conglomerate (f) Miocene marl . and (f) (e) Ophiolite-related harzburgite Post -ophiolite dome (f) (d) (b) Eocene volcanosedimentary northern grey dome of trachydacite exposed in 2356 2355 (b) Ophiolite complex and Post -ophiolite dome Contact between post-ophiolite subvolcanic rock and host Post-ophiolite dome (a) (b) Post -ophiolite dyke Ophiolite complex (e) (a) (c) Ophiolite complex Photograph of post-ophiolite dyke in the northern sector. Shaded relief image (after Shabanian et al., 2012) showing the location of Sabze- (c) Field photographs. ophiolite domes that outcrop insedimentary the and ophiolite Pliocene complex. conglomerates Eocene are volcaniclastic seen complex, Miocene in ophiolite-related harzburgite. harzburgite. shape amphibole aggregates in the andesitic dyke. Figure 1. (a) geological map of the(dash Sabzevar square) and area southern and (dotted the square) post-ophiolite sector of subvolcanic the rocks. study The area northern are indicated. var Ophiolitic Zone (SOZ). Lower leftlision/subduction inset framework. shows Black the arrows geodynamic setting andArabia-Eurasia of associated plate Arabia-Eurasia numbers col- movement represent velocities after the Reilinger present-day et al. (2006) in mm yr Figure 2. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | (f)

Rhyolitic fragments in the (d) Harzburgite belongs to ophio- (a) Flow texture and presence of acicular (a) Zoned plagioclase phenocryst in decite. Miocene marl. (e) (c) Euhedral to subhedral amphiboles with compo- 2358 2357 (b) association of amphibole aggregates and clinopyroxene (c) aceous siltstone. ff Eocene tu Field photographs of host rock xenoliths. Photomicrograph showing contact between crystal clot containing plagioclase (b) (d) Representative photomicrographs (XPL). amphibole and plagioclase in andesite. Figure 4. sitional zoning in trachyandesite. in andesite. Embayment and rounded quartz, altered sanidine and plagioclase in rhyolite. and amphibole and host trachyandesite rock. Figure 3. (a–c) lite complex. Pliocene conglomerate. Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | 2 5 5 7 5 7 7 Total alkalis 0 0 0 7 (a) 7 7 diagram. The fields 5 (j) 5 2 5 6 (f) 2 6 2 6 (c) O O i 2 O S Si Si adakites 2 2 0 0 0 O O 6 6 6 Andesite Si Si Lower crust-derived 5 5 5 5 5 5

Andesite

diagram (after Rollinson, 1993);

5 3 . 0 0 3 . 0 5 2 . 0 0 2 . 0 5 1 . 0 0 1 . 0 5 0 . 0 0 0 . 0 0 . 7 5 . 6 0 . 6 5 . 5 0 . 5 5 . 4 0 . 4 7 6 5 4 3 2 1 0

Mg# vs. SiO

2

Rb/Sr

r S b R O a C 2 O a N 5 5 5 7 7 7 (d) Lower crust-derived adakites Lower crust-derived Subducted- related adakites Subducted- related adakites Mantle melts (d) Trachyandesite (b) 0 0 0 7 7 7

O vs. SiO

Trachyandesite 2 O K 2 Mg ≠ Mg 5 5 5 2 6 2 K 2 6 6 O O (b) O (e) Si Si Si (h) (b) 0 2360 2359 0 0 Trachydacite 6 6 6 e t i l o y h HSA R Trachydacite 5 5

5 5

5 5

6 5 4 3 2 1

Dacite 0 0 0 2 0 5 1 0 0 1 0 5 0 6 4 2 0 8

Sr/Y

O g M

l a t o T O e F Y r S Peraluminous total FeO 5 5 5 7 7 7 Subalkaline Dacite 2 0 0 0 Rhyolite 7 7 7 O Alkaline Si A/CNK Rhyolite 5 5 5 2 6 2 2 6 6 O O O Peralkaline Si (a) (d) Si Si (g) 0 0 0 6 6 6 LSA NK diagram (Maniar and Piccoli, 1989); / (a) (c) Metaluminous 5 5

5 5

5 5

7 . 0 6 . 0 5 . 0 4 . 0 3 . 0 2 . 0 1 . 0 0 .

Figure 5 Figure 0

1 2 0 2 9 1 8 1 7 1 6 1 5 1 4 1 0 3 0 2 0 1 0 0 4

2

A/NK 6 Figure

O a N

2

O i

T Harker diagrams of the major oxides (wt.%) and incompatible element ratios vs. SiO Selected major element plots for the subvolcanic post-ophiolite rocks. 2 3 O l A N r Z b A/CNK vs. A Figure 6. for the studied rocks. Figure 5. vs. silica diagram after Le Basries et is al. after (1986). Irvine The and boundaryadakites Baragar between (HSA) (1971), alkaline are and and subalkaline the after se- fields Martin(c) of et low-silica al. adakites (2005). (LSA) and high-silica of subduction-related adakites and lower crust-derived adakites are from Guan et al. (2012). Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Y Y d d G G i Plot of Sr vs. i T T ) and southern r b r Z Z 0 0 (b) 8 8 m 9 m 9 1 S 1 S . l . l a O d a d and t 2 N t LSA N e e a n r n r u a u S S S N S + e s s e e C t e C i t

O i r

r d a d a a n L n L o o h C h C C K K t t a o a l o T l T p p r r b e b e d N i N d i p p HSA S S U U h h T T a (b) a B B

(d)

b b 0 2 4 6 8 10 12 14

(b)

R 3000 2000 1000 0 R

0 0 0 1 0 0 1 0 1 1 1 . 0 1 0 . 0 0 0 0 1 0 0 1 0 1 1

Sr (ppm) Sr s e t i r d n o h C / e l p m a S s e t i r d n o h C / e l p m a S erences between low silica adakites (dashed ff 2362 2361 Yb Yb Dy 1989 Dy 1989 McDonough McDonough and and Sun Sun

r S Mantle Mantle Normal andesite,dacite, rhyolite (ADR)

Sr (ppm) Y vs. Y for the studied rocks. Fields of adakite and arc normal rocks Adakite / Primitive Primitive plot plot Spider Spider (a)

Rb Th Nb La Pb Sr Nd Sm Ti Y Lu

Rb Th Nb La Pb Sr Nd Sm Ti Y Lu (c) 0 100 200 300 400 300 200 100 0 Plot of Sr (a) 0 10 20 30 40 Cs Ba U K Ce Pr P Zr Eu

Cs Ba U K Ce Pr P Zr Eu

Figure 8 Figure 0101000 100 10 1 0.1 .10111 0 1000 100 10 1 0.1 0.01

O (wt.%) showing the chemical di

Normalized REE and trace element patterns for the northern ( Sr/Y Sample/ Primitive Mantle Mantle Primitive Sample/ 2 Sample/ Primitive Mantle Mantle Primitive Sample/ ) subvolcanic rocks. Primitive-mantle and chondrite data are from Sun and McDonough Na d + and c field) and high silica adakites (dotted field) (after Castillo, 2012). Figure 8. (a) are from Petford and Atherton (1996) and Defant and Drummond (1990). CaO Figure 7. ( (1989). Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | (d) . Arrow 2 0 3 1 (a) 600 vs. Si per formula A K) Amphiboles in the Mg- 4 + 1 2. 3 . (f) 7 (b) 400 (d) (a) (Na 0.8 7 2 te ) fall in the Mg-hastingsite field. 3 e si + it g (f) e ) 3 n F 3 + Crystal clots

7 0.6 . e + Al≥ asti 6 F u) Distance from core (μm) u) f 6 VI f < A l Pargas ( -H 1. A g VI 200 (ap M ( Fe (ap 4 Mg 0.4 . Al Al

Al 6 Si (apfu) alkaline VI < V I IV

2 (Na+K) 1. Andesite 1 Al . 0.2 6 (c) VI calc-alkaline 0

8

8 0

.

1

1 8 . 0 6 . 0 4 . 0 2 . 0 0

0

2

3 4 0. 5 0 1 5 . 0

0 5 4 3 2 1

) u f p a ( e F

) u f p a ( 0. 0. 0. 0. K 0.

) u f p a ( ] K + a N [

3 + A

A

5

5.5 e te 4.5 t 2. i ai Trachyandesite (c) (e) nga ag 2364 2363 (a) da an a 4 7 5 6 S 6 - 2 g Sad indicates slope of 1. M

e

t

i te Tschermakite te

c 5.5 si Ferro- Tschermakite g te

a asi Al per formula unit and n

d si 5 g ) ) 6.5 g 3 )

y 3 (e) ) 3 + 1. + n te 3 + asti

h e IV

e + e -Par F

c e F -H F asi o ≥ ≥

F asti l

a r o u) < l g 5 l <

r r f . A l A -H er 0 A VI

T A er VI g <

( F VI 7 ( Par 600 F ( VI 5 A 1 . M ( ) Si (apfu) 6.5 1 (ap Si (apfu) K ≥ + B a Ferro- Hornblende te Al a i

N 5 C ( . Mg-Hornblende V I en 0

≥ te

5 i 5 A . 7.5 )

-ed 1 0. 5 K o en . ≥ r Dacite + 0 B a < (a) a (a) i Ed er N C ( T F 7.5

Ferro- Actinolite Actinolite

Termolite

8

1 8 . 0 6 . 0 4 . 0 2 . 0 0

1 8 . 0 6 . 0 4 . 0 2 . 0 0 0

2 1 0

9 Figure

400

) u f p a ( l A

) u f p a ( ] e F + g M [ / g M

) u f p a ( ] e F + g M [ / g M

I V

2 + 2 + Amphiboles in andesites with +2 Si Mg Al plotted against (b) Fe Distance from core (μm) VI 200 Back-scatter electron microprobe image of a representative amphibole phe- ) vs. Si classification diagrams (after Leake, 1978; Leake et al., 1997, 2004). (e) + 2 Major element traverses in multiple-zoned amphibole phenocryst from (b) Major element classification diagrams for amphiboles. Fe 0 + 1 5 4 2 0 3 (c) (Mg and Amphiboles in the trachyandesite, trachydacite and dacite samples and crystal clots on the / nocryst from a(b) trachydacite sample that comprises distinct alternating dark and light zones. Figure 10. (a) unit for amphiboles from all samples.Leake Procedure et for al. assigning (2004). Al Solid according black to line Leake (1978) in and indicates position of rim to core traverse. Scale bars represent 100 µm. Figure 9. andesite samples. (c) Mg Plot of AK vs. IVAlalkaline after field. Ridolfi and Renzulli (2012). Our calcic amphiboles located in the calc- Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | , (c) and . The errors T 8 2 )- and 2 O and MgO O f (b) f to An An 20 Log ( 60 40 0 20 (b) 212) in the feldspars sieve-textured plagio- 200 = (c) n 2 curves are from O’Neill and FeO + oscillatory zoned plagioclase with MgO 0 0 5 100 4 5 1 1 1 1 1 clots 0 (b) 0 1 1 2 1 Distance from core (μm) An% 0 0 5 5 0 0 Andesite 1 1

0 (e) 1 0 0 (c) %) 0 0

t 1 NNO 0 (w

0 t l 0.4 0 0.2 5 8 0.6 e 5 9 9 m 11.5 %). Our amphiboles plot in the field of ex- O T (°C) T T (°C) T Trachyandesite 2 0 0 H 0 9 ± 0.4 0.2 0.6 0.8 6

2366 2365 0 0 5 P zoning profiles showing variations in X 5 8 8 4 0 0 Trachydacite C, 8

(e)

◦ 600 NNO +2 NNO (c) (b) (a) 0 2 4 6 8 10 12 14 2 4 6 0 2 5 5 750 850 950 1050 1150 750 850 950 1050 1150 7 7 0 0 0 0 0 0 0 0 0 0 7 9 1 3 5 0 - - Dacite 5 5 5 5 5 0 0 0 0 950 1 1 1 850 750

5 0 5 0 1 0 9 8 7 - - -

1150

1050

500

1 1 2

1500 1 1 Figure 12 Figure 2000 (°C) T 1000 2 O ƒ g o L and P(MPa) 23.5

± 400 MgO (d) 0.8 wt.%). The NNO and NNO T ± ( An% FeO melt 200 O Distance from core (μm) 2 . Plagioclase in rhyolites from the south part range from An diagram for calcic experimental amphiboles after the Ridolfi and Renzulli 70 (d) (b) (b) 0 (a) T - 0 20 40 60 P Composition of all analyzed plagioclase data points ( diagrams for the studied amphiboles as obtained by amphibole thermobarometry and An melt 20 O 2 -H T 0.2 log unit) and H ± perimentally re-produced amphiboles (after Ridolfi and Renzulli, 2012). composition triangle. Plagioclase compositiontween in An the samples of the northern sector vary be- (c) after Ridolfi and Renzulli (2012).( This method indicates typical uncertainties for log Pownceby (1993). Figure 11. (a) BSE images of selected plagioclase phenocrysts show abrupt increasing in An contents (up to 15 mol %) toward the rim and clase mantled by highand An FeO rim. for the oscillatoryrespectively. zoned Yellow arrows plagioclase indicate and core the to sieve-textured plagioclase rim in profile. Figure 12. (a) (2012) with low uncertainties ( Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | ), respectively. Rhy- ), while the trachyan- 20 − Results of plagioclase- 50 30 −

(b) 70 Depth (km) Depth ). 10 0 0 3 6 9 − 15 0 12 1 1 20

Rhyolite

) and (An

- 0.11 -

9 +0.05 9 . 0 9 30 0 6 2 1.10

5 +0.11 − 9 7 . 2

0

0 out of equilibrium of out 1.05 5 1 50 Dacite 0 2 9 0 . 0 1 3 0 5 2 >1050 c° 7 1.00 8 1 . 2 0 equilibrium field 3 9 0.95 8 1 . 0 0 4 7 1

9

7 0.90 out of equilibrium of out . 5 0 1 0 0 <1050 c° 5 9

3

7

1 Kd= 0.10 Kd= equilibrium of Out 0.85 . 0 equilibrium of out T (°C) T 0 3 1 ) equilibrium field 1 1 7 C .

100×Mg≠ melt 0.80

9 Kd= 0.27 Kd= ° 2368 2367 0 ( 7

6 7 . 0 T 0.75 Observed Cpx component 0 2 5 3

0 6

0 .

8 3 Increasingly mafic melt 0 out of equilibrium of out 0.70

5 0 5 0 - 0.05 - (a) 0.7 0.8 0.9 1.0 1.1 analysed Cpx point numbers (n:29) 8 8 7 7 (c) (b) (a) . . . . AlO1.5x CaO/SiO2xNaO0.5 1 5 9 13 17 21 25 29 1 0 50 30 20 10 0 0 0 0 10 20 30 40 50 60 1 Trachydacite/trachyandesite 0.65 0 0 0 0 0 0 0 0 0 0 ...... 0 5 0 70- 50- 30- 20- 8 4 0 6 2 8 7 6 5 4 3 2 1 0 8 7 7 8 8 8 7 7

72 88 76 700 80 . . . 84 600 800 500 400 300 200

100

0.80 0.75 0.70 0 0 0

An An An An out of equilibrium equilibrium of out P (MPa) P Predicted Cpx component Cpx Predicted 100×Mg≠ Cpx 100×Mg≠ Figure 14 Figure (b) 0 0 (a) 7 700 800 900 1000 1100 700 800 900

0 0 0 0 0 0 0 ......

0 2 0 4 0 1 2 3 4 5 6 Andesite An/Ab

600 500 400

300 100 200 P (MPa) P Increasing An% Increasing 0 0.1 0.2 0.3 0.4 0.5 0 0.1 0.2 Test for equilibrium using predicted vs. observed clinopyroxene compo- (b) hedenbergite derived using the nominal equilibrium melt (basaltic andesite + Equilibrium test for plagioclase and four possible melts. The andesite sam- Test for equilibrium using the Kd[FeMg] between clinopyroxene and nominal melt 247 MPa. ± C and ◦ 36 Figure 14. (a) (basaltic andesite sample [no.0.27 N-1]). (Putirka, 2008). The result shows Kd[FeMg] values close to the ideal of nents of diopside dyke). Pressure calculated for selected clinopyroxenePutirka using (2008). clinopyroxene-melt barometry after ples appear to be in equilibrium with high anorthite plagioclase (An Figure 13. (a) desite/trachydacite and dacite are in equilibrium with (An olite, in turn, is in equilibrium with low anorthite plagioclase (An melt thermobarometry after (Putirka, 2008).± SEE for the plagioclase-melt thermobarometer are

Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Discussion Paper | Depth (km) Depth 21 0 3 9 24 27 6 15 18

12

0 3 N 0 45

Schematic illustration of the

5 2 (b) 30 Amph Alborz crust Upper crust Lower crust

Interaction with mantle wedge 0

magmatism 2 25 CPx Hydrated lithosphere Northern post- ophiolite subvolcanic

5 slab

Pl- melt barometery 1 Amphibole barometery Cpx-melt barometery Slab melting ) 20 2370 2369 C ° (

Frequency (%)

T 0 1

15 Moho Pl Northern subvolcanic domes

18–27 km depth. 5 (b) Middle crust (a) Asthenosphere Central Iran Crust Lithospheric mantle ∼ Sabzevar Ophiolite zone 10 0

45 60

S 30 15

Depth (km) Depth

Oligocene-Miocene? 0

0

0

5

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

9

8

7

6

5

4

3 2

Figure 15 Figure

1

1 Tectonic framework illustrating northward subduction of Sabzevar oceanic crust P (MPa) P P(MPa) 16 Figure A comparison of the results of amphibole, plagioclase-melt and clinopyroxene-melt 0 0 1 2 3 4 5 6 7 8 9 10 6–9 km and the other at ∼ Figure 16. (a) (eastern branch of Neo-Tethys) beneath eastern Alborz zone. magma plumbing system forbased subvolcanic on adakite-like the derived rocks thermobarometric in data. northern part of Sabzevar belt Figure 15. barometries that indicate two distinctof magma storage regions in the crust, one around a depth