The geochemistry and petrology of the ophiolitic rocks from the Kahramanmaraş region, southern Turkey

The regionally important dismembered ophiolitic sequence from the southern Kahramanmaraş region, located along the Arabian-Eurasian collision zone in southeastern Turkey, contains harzburgitic tectonites, ultramafic to mafic cumulates, isotropic gabbros and ophiolite-related metamorphic rocks. The ultramafic-mafic cumulate rocks are composed of wehrlite, lherzolite, olivine websterite, olivine gabbronorite, olivine gabbro and gabbro.

Turkish Journal of Earth Sciences http://journals.tubitak.gov.tr/earth/ Research Article Turkish J Earth Sci (2013) 22: 536-562 © TÜBİTAK doi:10.3906/yer-1203-1 The geochemistry and petrology of the ophiolitic rocks from the Kahramanmaraş region, southern Turkey Utku BAĞCI* Mersin University, Department of Geological Engineering, Çiftlikköy, TR-33343 Mersin, Turkey Received: 06.03.2012 Accepted: 19.09.2012 Published Online: 13.06.2013 Printed: 12.07.2013 Abstract: The regionally important dismembered ophiolitic sequence from the southern Kahramanmaraş region, located along the Arabian-Eurasian collision zone in southeastern Turkey, contains harzburgitic tectonites, ultramafic to mafic cumulates, isotropic gabbros and ophiolite-related metamorphic rocks The ultramafic-mafic cumulate rocks are composed of wehrlite, lherzolite, olivine websterite, olivine gabbronorite, olivine gabbro and gabbro The crystallization order of the cumulus phases, the presence of high Ca-plagioclase (An83–94), highly magnesian clinopyroxene (Mg#78–93), olivine (Mg#71–91) and their coexistence in the ultramafic-mafic cumulate rocks indicate a suprasubduction zone (SSZ) environment and suggest that the cumulates were derived from an island arc tholeiitic (IAT) magma The isotropic gabbros are mainly represented by hornblende gabbro, gabbro and diorite rocks The major and trace element geochemistry of the isotropic gabbros reveals two different magma types The first group is characterized by low TiO2 (0.91–1.52 wt.%) and Zr (35–79 ppm), and REEs exhibiting flat to slightly depleted LREE (LaN/YbN = 0.38 to 0.67) patterns, geochemically similar to island arc tholeiites The second group is characterized by higher TiO2 (2.67–3.87) and Zr (176–351 ppm) and displays significant LREE enrichment (LaN/YbN = 10.9 to 14.5) patterns, which are geochemically similar to oceanic island basalt (OIB) Metamorphic sole rocks are represented by alkali amphibolites and are similar to OIB All the evidence suggests that the ophiolitic rocks of the southern Kahramanmaraş region are associated with different types of magma generation and were emplaced onto the Arabian passive margin along the southern branch of the Neotethys oceanic basin during the Late Cretaceous Key words: Suprasubduction, island arc tholeiite, alkaline, cumulate, ophiolite, Turkey Introduction The geology of Turkey is linked to the evolution of the Tethys ocean, which is commonly subdivided into Paleotethys and Neotethys oceanic basins Different definitions and locations of these oceans have been used by different workers (Şengör & Yılmaz 1981; Ustaömer & Robertson 1994; Okay 2000; Stampfli 2000; Robertson et al 2004) The Anatolian plate of the Alpine-Himalayan orogenic belt comprises remnants of the Neotethyan oceanic basins, placed as E-W trending tectonic zones, between metamorphic massifs and/or platform carbonates The remnants of Neotethys, in structurally descending order, are represented by ophiolites, metamorphic soles and ophiolitic mélanges (Şengör & Yılmaz 1981; Dilek & Moores 1990; Dilek et al 1999; Floyd et al 2000; Robertson 2002) The Neotethys is composed of two oceanic basins: the northern and southern branches (Şengör & Yılmaz 1981) The remnants of the northern branch of the Neotethys include the İzmir-Ankara-Erzincan zone, the Inner Tauride Ocean and the Intra-Pontides, whereas the southern branch marks the Bitlis-Zagros suture * Correspondence: bagciu@mersin.edu.tr 536 (Figure 1) These ophiolites of the northern and southern branches were generated during the closing stages of the Neotethyan oceanic basins in the Late Cretaceous (Şengör & Yılmaz 1981; Robertson & Dixon 1984; Yılmaz et al 1993; Robertson 2000; Robertson et al 2006) Ophiolites, which have an important place within the Neotethys evolution of Turkey, are of the suprasubduction zone (SSZ) type (Yalınız et al 1996; Parlak et al 1996, 2000, 2002; Robertson 2002; Parlak et al 2004; Vergili & Parlak 2005; Bağcı et al 2005, 2006; Rızaoğlu et al 2006; Uysal et al 2007; Bağcı et al 2008; Bağcı & Parlak 2009; Parlak et al 2009; Sarıfakıoğlu et al 2009; Dilek & Thy 2009), and they display a consistent sequence of events during their formation and emplacement The southeast Anatolian orogenic segment of the Alpides, where the study area is located, can be divided into three approximately east-west-trending zones From south to north, these are the Arabian Platform, the imbricate zone and the nappe zone (Yılmaz 1993) The Arabian Platform, containing autochthonous sedimentary rocks that have accumulated with minor interruptions since the BAĞCI / Turkish J Earth Sci 20°E in ar id rZ eo ph Mirdita Ophiolite es lit io Pontide el le ni de s İzmir n cia Ly Aegean Sea s ppe AO Na T au r i d e AC Rhodes Crete Mediterranean Aegean Trench rth tf o rm ato lian Fau lt S Kahramanmaraş Cyprus Trench em em yst lt S Fau Guleman ophiolite s Suture Zone Baskil arc İspendereKömürhan ophiolite gro Bi Study area MO 40°N yst na A ast E an toli -Za tlis Troodos oph Sea An DO BHN Pl a 44°N 42°N Munzur ANATOLIA Z ES IA No a kar An lange Me VO H Küre ophiolite Çangaldağ arc s İstanbul 40°E Sea Black IPO PO 36°E Rhodope Massif on A dr Se iatic a Moesian Platform a rd Va es 32°E 28°E 24°E EURASIA Dead Sea Fault System D ARABIA 36°N Kızıldağ ophiolite 100 Km 34°N Figure Distribution of the Neotethyan ophiolites and major tectonic features in the eastern Mediterranean region (from Dilek and Flower 2003) AC: Antalya Complex; IPO: Intra Pontide Ophiolites; BHN: Beyşehir-Hoyran Nappes; İAESZ: İzmir-AnkaraErzincan Suture Zone; MO: Mersin Ophiolite; PO: Pindos Ophiolite; VO: Vourinous Ophiolite; AO: Aladağ Ophiolite; DO: Divriği Ophiolite early Paleozoic, also includes ophiolite nappes emplaced in the Late Cretaceous and their cover sedimentary rocks, ranging in age from Late Cretaceous to Miocene The Arabian Platform is divided into three units: the lower autochthonous, the upper autochthonous and the allochthonous units (Yılmaz 1993; Yılmaz et al 1993) The allochthonous units form a nappe package composed of two major groups of rocks The ordered ophiolites (Figure 2), observed in different places in Southern Anatolia at the top and bottom of the ophiolite, include two distinct and internally chaotic assemblages, which are separated by thrusts and emplaced on the platform during ophiolite obduction The stratigraphic thickness of the nappes is estimated to exceed km (Yılmaz 1993) Well-dated ophiolites in the Eastern Mediterranean are restricted to three well-defined, relatively brief time intervals: Triassic, Mid-Late Jurassic and Late Cretaceous (Robertson 2002) The geological history of the Mediterranean region was dominated by the opening of the Neotethys Ocean, mainly during the Early Mesozoic (Robertson & Comas 1998) During the Triassic period, one or several microcontinents rifted from Gondwana and drifted northwards, thereby opening a Mesozoic ocean basin (Şengör & Yılmaz 1981; Robertson & Dixon 1984) At the end of the Early Cretaceous period, depending on the opening of the South Atlantic Ocean, the divergent regime passed through the convergent regime in the Neotethys oceanic basin between the Eurasian and African plates (Livermore & Smith 1984; Savostin et al 1986; Dilek et al 1990, 1999) In this compressive regime, northward subduction occurred in the southern branch of the Neotethyan oceanic basin This oceanic basin was associated with the Upper Cretaceous genesis and emplacement of ophiolites (Yılmaz & Yıldırım 1996) Northward subduction of Neotethys caused the development of accretionary wedges in front of the Anatolide-Tauride Platform (Yılmaz & Gürer 1996; Robertson et al 2004) Before continental collision was initiated between the Anatolian-Tauride Platform and the Arabian Plate at the beginning of the Early Miocene (Karig & Kozlu 1990; Robertson et al 2004; Gül et al 2011), the nappe package advanced southwards and was emplaced onto the accretionary wedge and oceanic crust remnants at the end of the Oligocene period (Yılmaz & Gürer 1996) Recent studies of the Southeast Anatolian Orogenic Belt (Figure 2) are concentrated mainly on defining the internal stratigraphy, field relations and the geochemical features of the ophiolites and related units (Parlak et al 537 BAĞCI / Turkish J Earth Sci 390 370 360 390 380 410 400 420 39 Tunceli Baskil Sarız III EM Bitlis BM Maden PM IV II VI V Sivrice Malatya 380 Lake Van BM Gürün MM Siirt F Adıyaman EA Kahramanmaraş M İS İS -A M ND TS IR IN Diyarbakır Urfa EASTERN MEDITERRANEAN İs ke ba nde sin ru n 370 I SYRIA Thrust BM: Bitlis metamorphics Late Cretaceous nappe front PM: Pötürge metamorphics EM: Engizek metamorphics MM:Malatya metamorphics Miocene thrust EAF:East Anatolian fault MTS:Mountains Fault (Normal and strike-slip) I Kızıldağ ophiolite Antakya 36 - + II Göksun ophiolite Border folds III Berit metaophiolite Basement high 40 37 IRAQ Gaziantep COVER ROCKS Neogene-Quaternary sedimentary and volcanic rocks TAURUS RANGE Mainly platform carbonates Cover rocks NAPPE REGION Metamorphic massifs Mainly ophiolite V Kömürhan ophiolite UPPER NAPPE 36 LOWER NAPPE ZONE OF IMBRICATION Upper Maastrichtian-Lower Miocene Sequence ARABIAN PLATFORM Paleozoic Sequence IV İspendere ophiolite 80km N Mesozoic and Tertiary Sequence VI Guleman ophiolite 36 37 38 39 400 410 420 Figure Main tectonic units and ophiolites of southeast Anatolia (Yılmaz et al 1993) 2009) The well-documented ophiolites were formed in a suprasubduction zone environment in the southern branch of Neotethys in the Late Cretaceous However, few petrological and geochemical data are available for ophiolitic rocks in the southern Kahramanmaraş region (Yılmaz et al 1984; Kısakürek 1988) These ophiolitic rocks have not been differentiated or studied in detail and thus their geochemical and the tectonomagmatic significance is unknown Therefore, the aims of the present study are: 1) to present the geochemical and petrological features of ophiolitic rocks from the southern Kahramanmaraş region, 2) to compare the obtained results with the eastern Mediterranean ophiolites and 3) to emphasize the occurrence of the different types of ophiolitic rocks and their tectonic significance, related to oceanic crust generation in the southern branch of Neotethys Regional geology The southern Kahramanmaraş region (Figure 3), evaluated in this study, is located in the actively deforming East Anatolian Fault Zone, where a long-lived triple 538 junction (the Maraş Triple Junction) evolved as a result of the Alpine Orogeny (Karig & Kozlu 1990; Yılmaz 1993) The geological units of this region are classified into three groups These are: 1) Autochthonous Arabian Platform, 2) Ophiolite Nappes and 3) Tertiary Cover Units The Autochthonous Arabian Platform contains Lower Cambrian to Upper Ordovician limestone, with a sandstone, quartzite and shale alternation at its base These basement rocks are unconformably overlain by Upper Triassic-Lower Cretaceous dolomite and dolomitic limestone (Dubertret 1955; Atan 1969; Yılmaz et al 1984; Tekeli & Erendil 1986) The ophiolite nappes consist of three slabs that have tectonic contacts with each other The lowest one, the Karadut Complex (Late Triassic-Late Cretaceous), contains flysch and wildflysch containing clayey limestone with limestone, ophiolitic rocks, cherty shale and limestone This complex is overlain by the Koỗali Complex, which consists of ophiolitic mélange composed of ophiolitic blocks and epi-ophiolitic sedimentary rocks (Ylmaz et al 1993) The matrix of the Koỗali Complex contains serpentinite, mudstones of varying color with BAĞCI / Turkish J Earth Sci ı 42° 36° 30° ı 37° 00 00 ıı 36° 45 00 40° Ankara s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s UB 23-26 s s s s s s s s s s s s s UB s s17 s s s s s s UB 11 s s s s s s s s UB 14-16 s s s UB 12-13 s s s s s s s s s s s s s s Şerefoğlu s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s UB 19-22 s Karacasu s İzmir Van Kahramanmaraş Adana Mersin s Gaziantep 200 km U Pleistocene - Holocene s Alluvial Tortonian s s s s s s s s s 36° Hatay s s s Basaltic lava with tuffite TÜRKOĞLU GÖ Unconformity s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s NARLI ıı s s s s s s s s s s Emirler s s s s s s s s s s s s s s s s s s s s s s s s s s s s s Minehöyük A s s KALE DAĞI s s DA s s s s s ı 37° 20 00 Balıkalan UB UB 6-8 UB 2-3 ĞI s s s s s s s s s s s Kömürler s US s EM İR M Dolomite, limestone Unconformity Limestone, sandstone, quartzite and shale alternation Strike - slip fault SAKầAGệZ ỗerisu s s s UB 27-28 s s s UB 30-32 s s s s s s s s s s s s UB 29 s s s s s s s s s s s s s s s s s s s s s s s UB 33 s s s s s s s s s s s s s s s s s s s s s s s s s s UB 34 s s s s s s s s Hamidiye s s s s s s 370 09ı 00ıı L Cambrian - U Ordovician s s s s s s s s s s s s s ss s s s s s s Karadut complex: Cherty shale and limestone, clayey limestone, blocks of ophiolite and limestone Tectonic contact U Triassic - L Cretaceous ME ES Y AH SL Koỗali complex: Spilitic basalt, pelagic limestone, cherty limestone, (ophiolitic sheets in places) Tectonic contact L Triassic - L Cretaceous EG s Ophiolites: Undifferentiated harzburgite, dunite, serpentinite, gabbro Tectonic contact L Cretaceous ? s Unconformity L Cretaceous s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s NT ? ? s s s s s s s s s s GM SE s s Limestone, sandstone, siltstone, mudstone alternation U Maastrichtian - Paleocene T EN I AŞ LB Unconformity Dolomitic and sandy, chalky limestone U Paleocene - L Miocene ıı KAHRAMANMARAŞ İstanbul N Normal fault Undefined fault Overthrust Sample location and number s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s 10 Km s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s BÜYÜKDAĞ s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s UB 35 s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s s Figure Simplified geological map of the southern Kahramanmaraş region (modified from Herece 2008) radiolarites, cherts, shale and volcanics, which indicate a Late Cretaceous age (Yılmaz et al 1993) The ophiolites of the region tectonically overlie the Karadut and Koỗali Complex slabs, and are unconformably overlain by the Upper Maastrichtian-Paleocene limestone and sandstonesiltstone-mudstone alternations It has been reported (Herece 2008) that the Arabian Platform rocks (mainly Mesozoic limestone) were thrust over those ophiolites The Upper Paleocene-Lower Miocene units, comprising dolomitic, sandy and chalky limestone, discordantly overlie all older units (Gül 1987; Terlemez et al 1992) This unit is nonconformably overlain by the Tortonian Yavuzeli Basalt (Yoldemir 1987) The Upper Pleistocene-Holocene units overlie all the units with angular unconformity The ophiolitic rocks from the southern Kahramanmaraş region are highly dismembered and composed of undifferentiated mantle tectonites and gabbroic rocks (Figure 3) Cropping out throughout the study area, the highly serpentinized mantle tectonites are composed mainly of dunite and harzburgite, and display foliation and lineation, which reflect plastic deformation Pyroxenite dykes, ranging in thickness from 10 to 40 cm, cut the mantle tectonites The chromitites display a great variety of textures: massive, nodular, schlieren and disseminated (Uysal et al 2007; Uysal 2008) The cumulate rocks are defined as gabbroic cumulate and hornblendites north of Şeferoğlu (Figure 3) (Kısakürek 1988) Small-scale outcrops of the ultramafic-mafic cumulates, isotropic gabbros and amphibolites (see section on petrography) are limited by tectonic boundaries and seem to be irregularly dispersed in the study area The ultramafic-mafic cumulate rocks display an igneous layering lamination and graded bedding and include very thin pegmatitic bands (5–10 cm in thickness) The massive to weakly foliated isotropic gabbros are dark green and fine to medium grained The amphibolites have no pronounced foliation or schistosity along the contact with harzburgitic tectonites 539 BAĞCI / Turkish J Earth Sci Sampling and analytical methods Samples were collected from different ophiolitic units for petrographic and chemical analyses, mostly around Karacasu village (Figure 3) and south of the massif where preserved outcrops are found A total of 30 selected samples (3 ultramafic cumulates, 13 mafic cumulates, 12 isotropic gabbros and amphibolites) were analyzed for major and trace elements at ACME Analytical Laboratories Ltd., Vancouver, Canada Major element analyses were performed on solutions after LiBO2 fusion and nitric acid digestion of rock powder for inductively coupled plasma-atomic emission spectrometry (ICP-AES) Trace and rare earth element (REE) analyses were determined by inductively coupled plasma-mass spectrometry (ICPMS) after LiBO2 fusion and nitric acid digestion Loss on ignition (LOI) is calculated by the weight difference after ignition at 1000 °C Detection limits range from 0.002 to 0.04 wt.% for major oxides, 0.1 to 30 ppm for trace elements and 0.05 to 0.1 ppm for the REEs Mineral compositions were determined using a CAMECA SX-100 electron microprobe at the Department of Earth and Environmental Sciences, Section for Mineralogy, Petrology and Geochemistry of the Ludwig Maximilian University of Munich, Germany The analytical conditions are 15 kV accelerating voltage, 20 nA beam current and 10 to 30 s of counting time for silicates Raw data were revised by a PAP (Pouchou & Pichoir 1984) matrix correction Detection limits for the oxides are 0.02 wt.% for Si, Al and K; 0.03% for Ti, Mg, Ca and Na; 0.07% for Fe, Cr and Mn; and 0.10% for Ni Petrography The cumulates of the ophiolitic rocks from the southern Kahramanmaraş region are divided into ultramafic and mafic cumulates The ultramafic cumulates are composed of wehrlite, lherzolite and olivine websterite Lherzolite exhibits adcumulate texture (cf Wager et al 1960) and is dominated by cumulus olivine, clinopyroxene and orthopyroxene (Figure 4a) Olivine websterite displays similar cumulate to poikilitic textures Wehrlite consists of anhedral cumulus olivine, poikilitic clinopyroxene (Figure 4b), minor chromite and intercumulus plagioclase The mafic cumulate rocks are represented by olivine gabbronorite, olivine gabbro and gabbro The olivine gabbronorite presents mesocumulate texture and consists mainly of cumulus and intercumulus plagioclase, poikilitic clinopyroxene and orthopyroxene (Figure 4c) with olivine The olivine gabbros have mainly orthocumulate (Figure 4d) to mesocumulate textures with cumulus and intercumulus olivine, clinopyroxene and plagioclase The gabbros generally have mesocumulate texture (Figure 4e) represented by cumulus plagioclases and clinopyroxene, with orthopyroxene and amphibole as intercumulus 540 minerals Serpentine, fibrous actinolite, amphibole, sericite and kaolinite are the secondary phases in these rocks The isotropic gabbros have a granular texture and are composed of hornblende gabbro, gabbro and diorite The hornblende gabbros display granular texture and include subhedral to anhedral clinopyroxene, amphibole and plagioclase (Figure 4f) While the gabbro contains clinopyroxene and plagioclase, diorite contains amphibole and plagioclase (Figure 4g) Titanite and opaque (Fe–Ti oxide) minerals are accessory phases in these rocks The dark green amphibolites from the metamorphic sole display granoblastic texture and contain green hornblende (Figure 4h) The dominant order of crystallization in the cumulates is olivine ± chromian clinopyroxene→orthopyroxene→pla gioclase, typical of SSZs, while petrographic observations of the isotropic gabbros show crystallization of plagioclase before clinopyroxene, which is also typical of normal mid-ocean ridge basalt (N-MORB) A summary of the petrographic features of the ophiolitic rocks from the southern Kahramanmaraş region is given in Table Whole rock chemistry The major, trace and REE contents of the ultramaficmafic cumulates, isotropic gabbros and amphibolites are presented in Table The LOI values range from 5.9 to 12 wt.% for the ultramafic cumulate rocks, and from 0.7 to 6.8 wt.% for the mafic cumulate rocks, indicating variable degrees of serpentinization, whereas the LOI values range from to 2.8 wt.% for the isotropic gabbros and amphibolites (Table 2) The variations of some selected major and trace elements are presented in Figures 5a–5j SiO2, TiO2, P2O5, Zr and Sr not show any correlation with MgO (Figures 5a, 5b, 5e, 5f, 5i) Al2O3, CaO and Ga show negative correlations (Figures 5c, 5d, 5j), whereas Cr and Ni exhibit positive correlation against MgO (Figures 5g, 5h) The ultramafic cumulates are characterized by low TiO2 (0.01–0.07 wt.%), Al2O3 (0.53–5.63 wt.%), CaO (0.88–5.90 wt.%), Sr (7–23 ppm), Ga (0.6–4.4 ppm), V (72–107 ppm), Zr (0.8–2.2 ppm) and Y (0.2–2 ppm) and high MgO (25.21–38.99 wt.%), Fe2O3 (6.93–15.51 wt.%), Cr (527– 3989 ppm) and Ni (770–2244 ppm) contents, whereas the mafic cumulates are characterized by high TiO2 (0.10–0.69 wt.%), Al2O3 (10.33–18.75 wt.%), CaO (7.73–18.25 wt.%), Sr (40–312 ppm), Ga (7.8–11 ppm), V (126–1195 ppm), Zr (2.1–11.1 ppm) and Y (3.1–11.3 ppm) and low MgO (9.26–14.16 wt.%), Fe2O3 (3.46–14.16 wt.%), Cr (281–1567 ppm) and Ni (25–226 ppm) contents (Table 2) The REE concentrations of the ultramafic-mafic cumulates exhibit spoon-shaped REE patterns (Figure 6a), with LaN/SmN and SmN/YbN ratios ranging from 0.39 to 1.04 and from BAĞCI / Turkish J Earth Sci Cpx Cpx Opx Ol Ol Cpx Chr a 0.2 mm b 0.2 mm Opx Pl Cpx Pl Cpx c Ol 0.2 mm d 0.2 mm Pl Cpx Pl Amp Opq e 0.2 mm Cpx f 0.2 mm Opq Pl Amp Amp g 0.2 mm h 0.2 mm Figure Petrographic views of ophiolitic rocks from the southern Kahramanmaraş region: a) adcumulate lherzolite; b) poikilitic texture in wehrlite; c) poikilitic texture in olivine gabbronorite; d) orthocumulate gabbro; e) mesocumulate gabbro; f, g) granular texture in gabbro and diorite from isotropic gabbros; h) granoblastic texture in amphibolite 541 542 36°53′27″ 36°58′06″ 36°50′49″ 36°58′42″ 36°58′42″ 36°57′23″ 36°57′23″ 36°57′23″ 36°51′07″ 36°51′07″ 36°50′44″ 36°50′49″ 36°50′49″ 36°52′36″ 36°52′51″ 36°54′53″ 36°59′45″ 36°58′45″ 36°58′45″ 36°56′24″ 36°58′06″ 36°57′58″ 36°59′13″ 36°59′04″ 36°59′16″ 36°58′31″ 36°58′42″ 36°58′42″ 36°58′26″ 36°58′42″ 37°18′25″ 37°29′44″ 37°09′36″ 37°18′17″ 37°18′17″ 37°18′29″ 37°18′29″ 37°18′29″ 37°09′35″ 37°09′35″ 37°09′24″ 37°09′36″ 37°09′36″ 37°07′48″ 37°06′55″ 37°04′16″ 37°29′58″ 37°29′36″ 37°29′36″ 37°30′05″ 37°29′44″ 37°30′07″ 37°30′26″ 37°29′42″ 37°29′40″ 37°30′06″ 37°30′55″ 37°30′26″ 37°30′12″ 37°30′55″ Olivine websterite Lherzolite Wehrlite Gabbro Gabbro Gabbro Gabbro Gabbro Olivine gabbro Olivine gabbro Olivine gabbro Olivine gabbro Olivine gabbro Olivine gabbro Gabbro Olivine gabbronorite Hornblende gabbro Gabbro Hornblende gabbro Diorite Diorite Hornblende gabbro Diorite Diorite Gabbro Hornblende gabbro Gabbro Hornblende gabbro Amphibolite Amphibolite Rock type Adcumulate-poikilitic Adcumulate Poikilitic Orthocumulate Mesocumulate Mesocumulate Mesocumulate Mesocumulate Mesocumulate Mesocumulate Mesocumulate Orthocumulate Mesocumulate Mesocumulate Mesocumulate Mesocumulate-poikilitic Granular Granular Granular Granular Granular Granular Granular Granular Granular Granular Granular Granular Granoblastic Granoblastic Texture 20 25 20 20 20 15 25 30 55 50 40 30 50 30 30 30 20 45 45 40 45 40 35 35 30 30 30 35 35 45 15 35 40 30