Shallow intrusive directions of sheeted dikes in the Troodos ophiolite: Anisotropy of magnetic...

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Geosystems

Published by AGU and the Geochemical Society

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ArticleVolume 1

December 13, 1999Paper Number 1999GC000001

ISSN: 1525-2027

GeochemistryGeophysics

Geosystems

Copyright 1999 by the American Geophysical Union

Geochemistry and Intrusive Directions In Sheeted Dikes in the TroodosOphiolite: Implications for Mid-Ocean Ridge Spreading CentersHubert Staudigel, L. Tauxe, and J. S. Gee

Scripps Institution of Oceanography, University of California San Diego, California ([email protected])

P. Bogaard, J. Haspels, G. Kale, A. Leenders, P. Meijer, B. Swaak, M. Tuin, M. C. Van Soest,E. A. Th. Verdurmen, and A. Zevenhuizen

Free University Amsterdam, Amsterdam, Netherlands

Abstract. [1] Sheeted dikes at mid-ocean ridge volcanoes represent the link between deep magma production and storage pro-cesses and shallow processes such as volcanism and hydrothermal activity. As such, they are crucial for the interpretation of manyobservations at mid-ocean ridges or other volcanoes with pronounced rift zones, including topography, hydrothermal systems,petrology, and geochemistry. We carried out a structural, magnetic, and chemical investigation of a 4 × 10 km sheeted dike sectionin the Troodos ophiolite, Cyprus. On the basis of major and trace element geochemistry, we distinguish dikes that may be corre-lated with the basal high-Ti series (HTS) lavas from those of the overlying low-Ti series (LTS) lavas. All dikes studied are nearlyparallel to each other, with vertical or steeply dipping planes whose strike likely indicates the orientation of the spreading center.Anisotropy of magnetic susceptibility measurements suggests that the HTS and LTS dikes intrude in fundamentally differentways. HTS dikes reflect the intrusive behavior of dikes in the vicinity of a magma supply system and define ridge parallel intrusivesheets that radiate out from the magma chamber. LTS dikes show a bimodal, orthogonal set of intrusive directions, one shallow andone near vertical. Near-lateral propagating dikes provide a means for delivery of magma into distant portions of a rift system, andnear-vertical dike propagation directions are probably associated with feeder dikes to down-rift surface flows. Our study suggeststhat the types of dike intrusive behavior in the Troodos ophiolite may also be typical for “normal” mid-ocean ridges or other majorshield volcanoes with well-developed rift zones.

Keywords: mixing in oceans; trace elements; boundary scavenging; beryllium; lead; isotope tracers; gyres.Index terms: marine geochemistry; physical oceanography; minor and trace element composition; trace elements; geochemistry.Submitted April 12, 1999; Accepted July 14, 1999; Published December 13, 1999.Staudigel, H. L., et al., 1999. Geochemistry and intrusive directions in sheeted dikes in the Troodos Ophiolite: Implicationsfor mid-ocean ridge spreading centers, Geochem. Geophys. Geosyst., vol. 1, Paper number 1999GC000001 [7426 words, 6figures, 3 tables]. Dec. 13, 1999.

1. Introduction[2] Sheeted dike systems comprise a volumetricallysignificant portion of ophiolite complexes and arethought to comprise a comparable fraction of the oceancrust as well [e.g., Baragar et al., 1990; Alt et al., 1996;Francheteau et al., 1992]. The processes of dike emplace-ment are critical to understanding many aspects ofcrustal accretion at mid-ocean ridges. For example, dikeinjection at fast and intermediate spreading ridges maycontrol the distribution and longevity of hydrothermalsystems through the direct introduction of heat intothe extrusive layer or through enhanced permeabilityallowing access to deeper heat sources [Pollard, 1987;Wilcock and Delaney, 1996; Cherkaoui et al., 1997;Curewitz and Karson, 1998; Schiffman et al., 1990]. Dike

propagation behavior provides an indirect means ofexamining the state of stress at mid-ocean ridges [Pol-lard 1987] and, indeed, may also play an important rolein modifying the stress field [Rubin and Pollard, 1987].Finally, dikes serve as conduits for delivery of magmafor the entire extrusive layer, whereby a variety of pro-cesses may influence the spatial variability of lavas, in-cluding flow differentiation or magma mixing [Komar,1972; Garcia et al., 1989] or the distribution of magmathrough lateral dike propagation [e.g., Sigurdsson, 1987;Baragar et al., 1990; Embley and Chadwick, 1994].

[3] Despite its potential importance for ridge crest ac-cretionary processes, relatively little is known aboutdike propagation at mid-ocean ridges. Early studiessuggested that dikes intruded vertically upward from

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nearly continuous mid-ocean ridge magma chambers[Kidd and Cann, 1974; Kidd, 1977]. Experimental stud-ies led to the suggestion of lateral dike propagation ina vertical plane along the rift zones of Hawaiian shieldvolcanoes [Fiske and Jackson, 1972] and, by analogy,along the ridge axis in ocean crust analogues such asthe Troodos ophiolite [Baragar et al., 1990]. Direct ob-servational evidence for lateral dike propagation islargely based on the progression of seismic swarms atactive volcanoes with well-developed rift zones on Ice-land and Hawaii [Sigurdsson, 1987; Rubin and Pollard,1987] and the Juan de Fuca Ridge [Dziak et al., 1995].Observations in the geological record have been car-ried out using a variety of structural, magnetic, and pet-rographic techniques [Baer and Reches, 1991; Knightand Walker, 1988; Philpotts and Asher, 1994]. In thispaper, we hope to contribute to the understanding ofthe intrusive behavior of dikes at mid-ocean ridges byusing a particularly well-known dike swarm in the geo-logical record, the sheeted dikes in the Troodosophiolite in Cyprus. A combination of chemical dataand flow directions of dikes based on anisotropy ofmagnetic susceptibility (AMS) measurements showsthat different chemical types show distinct intrusiveprocesses that may serve as a model for the behaviorof sheeted dikes at mid-ocean ridges.

2. Geological Background[4] Geochemical data from the Late Cretaceous (~90Ma) [Mukasa and Ludden, 1987] Troodos ophioliteprovide evidence for generation of this ophiolite in asuprasubduction zone spreading environment[Miyashiro, 1973; Robinson et al., 1983; Schmincke etal., 1983; Rautenschlein et al., 1985]. Nonetheless, thegross lithological layering, structure, and hydrothermalprocesses in this environment are considered to beanalogous to those of modern ocean crust [Moores andVine, 1971; Varga, 1991], implying that accretionary pro-cesses in the two environments are similar. In particu-lar, the uniform NNW strike of sheeted dikes overmuch of the ophiolite exposure (~30 km along strikeand 100 km orthogonal to strike) requires a spreadingenvironment on the scale of “normal” mid-ocean ridges(Figure 1). In the south and east portion of theophiolite, dike strikes gradually become more easterlyin the vicinity of the E-W striking Arakapas fault zone,widely interpreted as a fossil transform fault [Gass,1968; Moores and Vine, 1971; Gass et al., 1994]. Expo-sures in the ophiolite therefore provide an opportu-nity to examine the intrusive behavior of dikes in sev-eral structural settings that are similar to those at mid-ocean ridges.

Nicosia

Larnaca

Limassol

Paphos

32˚30' 33˚30'33˚00'

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ExtrusivesSheeted DikesPlutonicsLimassol Forest Complex

Arakapas Transform

Troodos

Troodos Ophiolite Cyprus

Arakapas Transform

Study AreaMassive Sulfide Deposits

Kampia Mine

Troodos

Figure 1. Simplified geological Map of the Troodos Ophiolite, Cyprus. The Limassol Forest Complex includes submarineextrusives and ocean crustal intrusives, separated from the Troodos ophiolite by the Arakapas Transform Fault. Thebox indicates the location of our study area that is illustrated in Figure 5. Modified from Bednarz [1989].







[5] For the present study, we selected an area alongthe Onouphrious and Pedhieos Rivers that offersnearly continuous exposure of dikes within theextrusive section and through a significant portion ofthe sheeted dike complex (see Bednarz [1989]; Bednarzand Schmincke [1987, 1994] and Schmincke andBednarz [1990] for a detailed description of the north-ern portion of the region; Figure 1). The sampling areaextends for ~10 km parallel to the dominant strike ofthe dikes (here NNE), to within ~10 km of theArakapas transform fault. Transform faults often rep-resent major geochemical boundaries, and they arelikely to pose some form of boundary to magmatic sys-tems as well [e.g., MacDonald and Fox, 1988; vanAvondonk et al., 1998]. Understanding the direction ofmagma flow in sheeted dikes relative to a transformzone is likely to help us understand how magma gen-eration processes are influenced by major structuralfeatures in the lithosphere. The northern portion of thestudy area also includes a large (> 500,000 tons [Vargaand Moores, 1985]) exhalative sulfide deposit hostedin pillow lavas near Kampia. These ore deposits revealthe deep sources of heat that may plausibly be linkedto the same intrusive centers that feed the dikes hostedby the overlying lavas. Dikes in the vicinity of such de-posits would be expected to deliver melt upward, andpossibly outward, from these suspected intrusive cen-ters. The goal of this study is to illuminate dike intru-sive mechanisms at this constructive plate margin inthe context of known spatial relationships to a hydro-thermal system and with well-constrained relationshipsto a transform fault zone.

3. Methods[6] All dike propagation directions in this study arebased on analysis of the anisotropy of magnetic sus-ceptibility (AMS) for at least five oriented samplescollected within ~10 cm of a dike margin. We have cho-sen this sampling approach because detailed analysisof a shallow dike revealed that magmatic flow in theinterior portions of some dikes can be disturbed bylate stage magma redistribution and/or rising vesicles[Staudigel et al., 1992]. Although flow patterns in dikesoften vary considerably with position in a dike orthrough time [Rickwood, 1990; Philpotts and Asher,1994], we regard the directions determined from near-margin samples as representative for magma flow dur-ing, and shortly after, crack propagation. It is likely thatthe initial propagation and magma flow direction alsorepresents the main magma feeding direction, but this

may not strictly be true in all cases.

[7] Mean flow directions and associated uncertaintieswere determined in 256 dikes using the bootstrappingtechnique of Tauxe et al. [1998] (see Appendix, Table1). Independent estimates of flow directions from mac-roscopic flow indicators (e.g., elongate vesicles, dikesurface lineations) as well as trachytic textures are wellcorrelated with the maximum eigenvector determinedfrom the AMS tensor [Varga et al., 1998]. Our dataanalysis scheme therefore eliminated sites whose maxi-mum and intermediate eigenvalues could not be dis-tinguished as well as sites with maximum principaleigenvectors > 45° from the dike margin (inverse fab-ric of Rochette et al. [1991]) or where the rakes of maxi-mum eigenvectors from opposite margins differed bymore than 30°. Overall, nearly three quarters of thedike samples yielded either unique flow directions orflow lineations [Tauxe et al., 1998]. In our analysis weused exclusively data from margins that display uniqueflow directions, i.e., where the maximum eigenvectorwas statistically distinct from the dike plane.

[8] Most dikes in the Troodos ophiolite have experi-enced some structural rotation after emplacement, ne-cessitating structural correction prior to the interpre-tation of flow directions. We largely followed the se-quential correction scheme of Varga et al. [1998], in-cluding, in particular, a correction for the northwardtilt (~10°) from doming of the ophiolite and restora-tion of the average dike attitude in each region to ver-tical by rotation about the average dike strike. Intru-sive directions of dikes within the dike plane (i.e., flowrakes) were obtained by projecting the maximumeigenvector onto the dike plane, and these directionsare plotted as rose diagrams in Figure 2. Characteris-tic remanent magnetization directions after structuralcorrection are invariably near the expected Troodosmean direction (274°/36° [Clube et al., 1985]), provid-ing support for the validity of this correction scheme[Varga et al., 1998]. We note, however, that estimatesof paleohorizontal are subject to potentially significantuncertainty. For example, the axis of structural dom-ing is close to the pole of the dike planes, so thatpaleohorizontal is poorly constrained for deeper por-tions of the dike complex far from sediment exposures.

[9] We determined major element compositions ofglassy dike margins by electron microprobe (Appen-dix, Table 2a) and bulk rock samples by X-ray fluores-cence (Appendix, Table 2b). All analyses were per-formed at the laboratories of the Free UniversityAmsterdam using a JEOL Microprobe (JXA-8800M)







and a Philips PW 1404 sequential X-ray spectrometer.Microprobe analyses were carried out on multiple glasschips, avoiding hydrated margins or phenocrysts, us-ing wavelength-dispersive analysis, with a 20 µm elec-tron beam, and an acceleration voltage of 15 kV.Lamont glass standard JDF — D2#2 was used for cali-brations for Si, Al, Fe, Mg, and Ca, and to evaluate in-strument drift during electron microprobe analysis[Reynolds and Langmuir, 1996]. XRF analyses for ma-jor elements were carried out on whole-rock powders,fused with Li2BO2 and Li2B4O7. Trace elements wereanalyzed using pressed powder pellets. Data qualitywas assessed using international rock standards (Ap-pendix Table 2b) [Verdurmen and Broekema-Roomer,1994; Potts et al., 1992].

4. Results

4.1. Distinguishing HTS Dikes From LTSDikes

[10] On the basis of compositions of unaltered glassyselvages of pillow lavas, the extrusive section of theTroodos ophiolite may be divided into two composi-tionally distinct series of lavas: (1) an upper low-Ti se-ries (LTS) of basaltic-basaltic andesites, depleted in in-compatible elements, and (2) a high-Ti series (HTS)of basaltic andesites to rhyodacites at the base of theextrusives that is less depleted in incompatible ele-ments (Figure 3) [Schmincke et al., 1983; Robinson etal., 1983]. These two series are about equal in eruptive

(d) LTS Dikes

(b) Margins withChemical Data

Up

N10 20 300

N

Down

0 5 10 15

(c) HTS Dikes

S

Down

0 5 10 15

(a) Margins Measuredby AMS

S

Up

10 20 300

Figure 2. Flow directions inferred from anisotropy of magnetic susceptibility measurements in Troodos sheeted dikes.The rose diagrams include all margins measured (a, from Tauxe et al. [1998]), the subset of samples from the Pedhieosand Onouphrious region, analyzed here for major element composition (B), and separate rose diagrams for HTS Dikes(C) and LTS Series dikes (D).







volume and well separated in their chemical composi-tion. Rautenschlein et al. [1985] analyzed a set of freshglasses from both series for trace elements and radio-genic isotopes and demonstrated that the magmaticsource regions of the Troodos ophiolite are isotopicallyand chemically heterogeneous. Similar conclusions canbe drawn for the sheeted dike section that appears tobe cogenetic with the lavas on the basis of their struc-tural relationship and chemical similarity. Baragar etal. [1990] analyzed a large number of dikes from theentire Troodos ophiolite and showed that they displaya continuous and slightly larger range in major ele-ment compositions, i.e. slightly shifted toward highMgO, but with a less well defined overall trend [Baragar

et al., 1990] (Figure 3). The more diffuse trend in bulkrock composition relative to glass compositions maybe largely attributed to the fact that Baragar et al. [1990]analyzed bulk rock powders. In such samples, seaflooralteration and metasomatic processes cannot be ex-cluded, and additional chemical deviation from liquidcompositions may have been caused by phenocryst ad-dition or removal [e.g., Staudigel and Bryan, 1981]. Fur-thermore, Baragar et al. [1990] pointed out that LTSdikes are much less abundant and that they do not fol-low the simple age sequence from HTS to LTS butlikely are contemporaneous.

[11] We have analyzed 77 glass samples from thequenched margins of dikes in the uppermost dike re-

Figure 3. SiO2 and TiO2 versus MgO for dikes from the Troodos Ophiolite. Data include XRF analyses of bulk rocksanalyzed for AMS and a large number of glass analyses of chilled dike margins in the wider Kampia Mining district(Tables 2a and 2b). We provide fields for the bulk rock data of Baragar et al., [1990] and the HTS and LTS extrusiveglasses of Robinson et al. [1983] and Schmincke et al [1983]. We plotted our own glass analyses, from a large numberof chilled dike margins in the wider Kampia.

0

50

60

70

0 2 10

0

1.0

2.0

MgO

SiO

TiO

2

2

HTS lavas

LTS lavas

Dikes fromBaragar et al, (1990)

Dikes Glassy Margins

Dikes Bulk Rocks

LTS lavas

HTS lavas

Dikes from Baragar et al., (1990)

4 6 8 12 14







gion near Kampia and 87 bulk rock samples from ar-eas throughout the entire region and plotted theseanalyses in a Harker diagram (Figure 3). Our datacover a large fraction of the previously known rangefor glasses and bulk rocks, missing only the most ex-treme end-members. In this study, we follow Baragaret al. [1990] and Bednarz and Schmincke [1994] anddefine LTS dikes as having TiO2 < 0.85, MgO > 5.5,and Cr > 40 ppm. Most samples can be uniquely beclassified using TiO2 and MgO alone, and the few re-maining transitional samples were classified on thebasis of Cr abundances.

4.2. Intrusive Directions of Dikes as a Functionof Chemical Rock Type

[12] Dike intrusive directions in the Troodos ophioliteshow a wide range, including vertically upward direc-tions as well as horizontal directions toward the south(Figure 2a) [Staudigel et al., 1992; Varga et al., 1998;Tauxe et al. 1998]. In Figure 2b we present the rose dia-grams for all the dikes that have meaningful magmaflow directions and chemical data. Overall, the distri-bution of dike flow directions is similar, even though apeak of south and up directions appears to be morestrongly developed in the sample set for chemicalanalyses.

[13] Dike propagation directions are quite different for

different rock types, confirming suggestions of Baragaret al. [1990] that they are likely to have been fed fromdifferent plumbing systems. Figure 4 shows two typesof distributions of dike intrusive directions. Nearly con-tinuous variation with a maximum of up/south direc-tions is observed at higher TiO2 abundances, and a bi-modal distribution of intrusive directions is observedat low TiO2 contents. It is quite curious that the minimabetween the modes of the LTS distribution (up andsouth directions) coincide with the highest density ofpoints in the HTS group. It is also interesting that thischange in distribution type appears to coincide veryclosely with the separation of HTS from LTS dikes atTiO2 = 0.85 wt %, in a relatively sharp change in dis-tribution. The physical observation of distinct dikepropagation directions corroborates Baragar et al.’s[1990] chemical arguments that HTS and LTS basaltsmay be related to different magmatic systems.

[14] Using this separation at 0.85 wt % TiO2, we plot-ted two separate rose diagrams for HTS and LTS dikes(Figures 2c and 2d) showing that they have fundamen-tally different intrusive directions. HTS dikes show upand south directions, while LTS dikes display a bimo-dal distribution of two orthogonal directions. The mini-mum between the orthogonal set of LTS dikes coin-cides with the maximum of HTS dike propagation di-rections. Such a distribution of dike intrusive directionscan be taken as an indication for two distinct plumb-

Figure 4. Ti content versus the rake of the maximum eigenvector from the AMS ellipsoid. Both dike margins are plottedseparately where both flow directions could be inferred. Note the sharp boundary in rake distribution for dikes aboveand below TiO2 = 0.85. LTS dikes display a bimodal distribution with a minimum in rakes where HTS dikes show amaximum of values in a very broad distribution.

North

Down

South

Up

North

0.25 0.50 0.75 1.0 1.25 1.50TiO

Eastern MarginWestern Margin

LTS Dikes

HTS Dikes

2

HTS Dikes







ing systems between these two magmatic series.

4.3. Spatial Relationships and Structure

[15] Hypothesizing that the two magmatic suites areactually fed from two distinct plumbing systems, weevaluate the distribution of dike propagation directionsin the context of their spatial distribution. We dividedour main study area into three regions (north, middle,south) that are distinct with respect to their strati-graphic position as well as their position along strikeof the spreading axis. The northern region includes pri-marily dikes within the extrusive series. This region alsohosts the Kampia massive sulfide deposit (see crossedhammer symbol in Figure 5) that suggests a zone ofsignificant convective heat removal, possibly supported

by an underlying intrusive complex. Dikes are rela-tively common (<10% of the exposures) near the mas-sive sulfide deposit and much less frequent in the north-ern portion of the Pedhieos and Onouphrious Canyons,where dikes constitute < 1% of the outcrop. The middleand southern regions lie within the sheeted dike com-plex (<95% dikes). The middle region is proximal tothe Kampia mining district, and it probably representsthe upper 300 m of the sheeted dike complex (on thebasis of an originally horizontal layered ophiolitestratigraphy that has been tilted uniformly by 10° tothe north). The southern region is farthest away fromthe Kampia mining district and closer to the Arakapastransform fault (~10 km to the south). Its stratigraphicposition is difficult to assess, but the significant verti-cal relief (~300 m), and the absence of pillows on the

Figure 5. Map of the study area with dike intrusive directions, presented in rose diagrams for three distinct regions, thenorthern extrusive section, the upper sheeted dike section and the southern middle sheeted dike section. The thick redline indicates the strike of the sheeted dikes, the Kampia mine is indicated by a crossed hammer symbol. Note that mostof the samples come from the fresh exposure along the Onouphrious and Pedhieos Canyons (blue lines) and the averagestrike of dikes gently curves from NNE trending dikes in the north to NE trends in the south of the area. This trendcontinues to almost westerly trends near the Arakapas transform fault (not shown). Roads are indicated as thin redlines. Samples are given as dots (blue HTS, green low Ti, yellow not analyzed).

36˚00'

36˚58'

35˚56'

Kionia Peak

S

Up

0 5

Down

10

Pedhieos River

OnouphriousRiver

HTS - Dikes LTS - Dikes

0 5

Up

Down

50 10S

Up

0 5 10

Down

S

0 5 10

Down

Up

N

0 5 10

Down

Up

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0 5 10

Down

Up

N

N

33˚14'33˚12'







top and gabbros at the bottom of the section, suggeststhat it is likely to be stratigraphically lower than themiddle region, somewhere in the middle of the dikesection.

[16] Each of these regions also has a characteristic di-rection of dike propagation for HTS and LTS dikes. Inthe northern extrusive region, LTS and HTS dikes donot show intrusive behavior with clear directional pref-erence, even though southerly and upward intrusivedirections appear to be particularly common (Figure4). Dikes in this area are emplaced well above thesheeted dike complex, and their intrusive behavior islikely to provide insights mostly into the growth andinternal stress field of mid-ocean ridge volcano edi-fices rather than the deep ridge structure. However,the number of dikes studied is too small to provideenough clues to understand the role of dikes in thegrowth of these particular volcanoes.

[17] In contrast, HTS and LTS dikes within the sheeteddike complex display well-defined flow distributions,although flow directions in these two geochemicalgroups are distinct. HTS dikes in the middle and south-ern region show simple upward distributions of flowdirections. Flow was dominantly vertical in the middlearea, whereas the southern area is characterized byoblique flow directions (southward and up at ~50°).LTS dikes from both the middle and southern areasconsistently display a bimodal distribution of intrusivedirections that are at an angle of ~90°. The majority ofLTS dikes exhibit shallow upward flow directions(~30°) toward the south, with a somewhat smaller num-ber of dikes having moderate (40°–60°) flow directionsupward toward the north. Although the number ofdikes is small, intermediate directions are conspicu-ously absent.

5. Discussion[18] The main discovery from this study is that dikes inTroodos display a wide and continuous range of propa-gation directions on a large scale, but this diffuse pat-tern breaks down into well-defined patterns when dikepropagation is placed in the context of a particular lo-cation and chemical type. Our data suggest that differ-ent chemical types are fed from different magmaplumbing systems and that different locations with re-spect to a spreading center volcano determine the di-rection of magma transport. We believe that this dis-tribution of flow directions provides us with some in-teresting clues regarding the intrusive behavior of dikes

at mid-ocean ridges. However, before this can be donewe have to discuss the effects of structural correctionsmade in attempting to restore the dikes to their origi-nal orientations.

[19] Among the structural corrections applied, thenorthward tilt related to doming most directly affectsthe rake determinations in these NNE striking dikes,yet this correction is the one that is least well con-strained. To accommodate for doming, we applied auniform adjustment of 10° that is based on the dip ofsediments near the pillow-sediment contact near ourstudy area. This procedure has been used successfully[Varga et al., 1998], but it effectively treats doming as ahomocline. This is an oversimplification, because dom-ing, in its ideal geometric expression, displays zero tiltat the center of the dome, maximum tilt on its flanks,and zero tilt in the far field. Thus we expect the tilt toincrease as we approach the doming area from thenorth and then decrease again as we approach the cen-ter of uplift. Behavior similar to this is observed in thesediments with dips of about 5° four kilometers northof the ophiolite that increase to about 10° at the sedi-ment-pillow contact. Thus a further increase in dom-ing-related rotation is likely as we approach the cen-ter of uplift that is located about 10 km farther south.However, the exact center of uplift and total amountof uplift are very difficult to constrain. Gabbros east ofKionia suggest that it represents the mid to lower por-tion of the dike swarm. From this one might add uptopographic relief and the thickness of the overlyingophiolite to determine an average (“homoclinal”) dipof about 25° between Kionia Peak and the top of thepillow section. If this is correct, the actual rotation atintermediate distance between the center of domingand the pillow complex is likely to be significantlyhigher, possibly of the order of 40°. Rotations of thisorder of magnitude or larger are not unusual in igne-ous sequences, including many ophiolites, but they tendto be difficult to constrain because of a lack ofpaleohorizontal indicators.

[20] For this reason, one might argue that the appliedadjustment of 10° is a minimum rotation but that a ro-tation exceeding 40° is possible, at least in some por-tion of the ophiolite. Such a rotation would bring theAMS dike propagation direction for the LTS dikes intohorizontal southern and vertical upward direction. Totest this, we determined the characteristic remanentmagnetization directions in a representative set ofsamples from the north, middle, and southern regionand rotated these samples by additional doming to







bring the AMS propagation directions into horizontaland vertical directions. This procedure does indeedbring the observed rock magnetizations of the middleand southern portions closer to the directions of thenorthern segment, consistent with the above sugges-tion of steepening of the segments deeper in the sec-tion. However, the data are insufficient to demonstratesignificant improvement of fit when compared to theoriginal rotation of 10°. We therefore regard a 40° ad-justment as plausible but not proven.

[21] Considering these observations and inferences, wecan imagine a vertical-horizontal pair of intrusive di-rections for the LTS. Such a distribution appears likelyfrom observations at large volcanoes with prominentrift zones (Kilauea, Krafla) or volcanoes that are asso-ciated with rifting or oceanic spreading centers. Verti-cal upward flow directions are required for feeding sur-face lava flows from depth, and a matching horizontalorthogonal set is inferred from a series of seismic, geo-logic, and magnetic observations [Sigurdsson, 1987;Rubin and Pollard, 1987; Dziak et al., 1995; Ernst andBaragar, 1992; Staudigel et al., 1992]. For these reasons,we interpret the bimodal distribution of intrusive di-rections in LTS dikes as being typical for the distantbehavior of sheeted dikes in rift zones. Horizontal flowdirections indicate lateral magma transport toward theArakapas transform, and vertical upward flow direc-tions indicate feeders of rift zone eruptions.

[22] An interesting consequence of the rotation of theLTS dikes is that the HTS dikes must also be rotated,

simply because they are in the same structural unit andbecause cross-cutting relationships indicate overlap-ping periods of emplacement [Baragar et al., 1990]. Inthis case, the upward peak in the middle area will havea southerly upward direction, and the southern HTSdikes become closer to horizontal. As a result of thisrotation, the inferred intersection of flow directionsfrom these dikes will move northward, closer to andpossibly beneath the Kampia massive sulfide deposit.This is consistent with the interpretation that theKampia massive sulfide deposit is a center of intrusiveactivity for the HTS lavas, further evidence for an in-ternally consistent interpretation of the dike intrusivedata presented here.

[23] Drawing together these constraints and conjec-tures, we can summarize our data in a rather simpleway, as illustrated in a sketch in Figure 6. HTS dikesand LTS dikes show quite different dike propagationdirections. HTS dikes appear to reflect the intrusiveactivity of dikes near an inferred major deep magmasupply. Here, dikes maintain the near vertical and par-allel attitude of the sheeted dikes, but they areemplaced radially within that plane. The angle of em-placement is steep above the magma chamber and atshallower angles in the more distant portions of thevolcano. LTS dikes, however, reflect the distant flowfield of dikes relative to the volcano, whereby effec-tively horizontal feeder dikes supply the rift zones withmagma, and occasional vertical upward branches ofmagma flow directions are necessary to supply the sat-

Figure 6. Cartoon illustrating the propagation behavior of dikes in a schematic ocean crustal section, includingextrusives (top, green), dikes (middle, with arrows) and an intrusive body (bottom, red, with crosses). LTS dikes (yellow,left) intrude in vertical sheets, laterally away from the intrusive center, with occasional surface eruptions. This eruptivepattern results in a bimodal distribution of intrusive directions including horizontal and vertical intrusive directions.HTS dikes also intrude in vertical sheets that are parallel to the ridge axis, but intrusive sheets radiate out from acentralized magma reservoir, near vertical above the magma chamber and shoaling away from the reservoir.

2 km

4 km10-25 km

High Ti DikesLow Ti Dikes

to Transform

2 km







ellite vents on the rift zones with magma.

[24] There are several structural and chemical obser-vations made by Baragar et al. [1990] that are relevantto our interpretation. These include, in particular, theobservation that LTS dikes and HTS dikes arepenecontemporaneous and the fact that HTS dikes aresubstantially more abundant than the LTS dikes (seeFigure 4). This contrasts with the behavior of theTroodos lavas that show roughly similar volumes anda clear temporal sequence from HTS to LTS lavas.Baragar et al. [1990] suggested that HTS and LTSmagma systems alternate along the ridge axis and dikesare emplaced penecontemporaneously through lateraldike injection. Our study suggests that the HTS dikesare local, while the LTS dikes come from a greater dis-tance to the north. The differences in abundance ofdikes and lavas require very voluminous eruptions ofLTS lavas where a relatively small number of dikesproduces a large volume of lavas. HTS dikes producerelatively small volumes of extrusives for a given dikevolume, whereby it is very likely that many dikes maynot produce any lavas. This interpretation is also con-sistent with the higher viscosity calculated for the HTSlavas by Bednarz and Schmincke [1994]. Low melt vis-cosities allow for rapid transport and extrusion. Whilethese obervations round off our understanding of theintrusive behavior of sheeted dikes in the Troodosophiolite, they also have to be considered when apply-ing our data to other ridge settings as well where di-verse magma compositions can be found.

[25] This study illuminates the intrusive behavior andmelt transport phenomena in the Troodos ophiolite,and this example may be extrapolated to volcanoes at“normal” mid-ocean ridges or intraplate volcanoeswith prominent rift zones. HTS dikes are derived froma magmatic intrusive center that underlies the Kampiamassive sulfide, relatively close to the Arakapas trans-form fault, and possibly provides the heat responsiblefor the hydrothermal system. The source of the LTSdikes appears to be located to the north of the studyarea, and LTS dikes in this region reflect the more dis-tant parts of a mid-ocean ridge (MOR) volcano. Thisinference would suggest that in this region, the under-lying mantle has produced mostly HTS melts, while themantle farther north has produced the LTS melts. Theselocal complex relationships between dike chemistryand intrusive geometry show that extrusives found atany particular location along a ridge may be controllednot only by a local control on partial melting and meltcomposition but also by along ridge transport. Any par-

ticular submarine extrusive sample from a locationalong a mid-ocean ridge may reflect the mantle com-position from a distant centralized region of mantleupwelling. These observations shed some new light onthe discussion of along-axis chemical variations at mid-ocean ridges and the relationships between extrusivechemistry (Ti content) and melting behavior in vicin-ity of a fracture zone [e.g., Bender et al., 1984; Langmuirand Bender, 1984; Karson and Elthon, 1987]. This showsthat the magma plumbing systems of MOR volcanoesneed to be understood before physical relationshipscan be established between a particular sample loca-tion and underlying mantle chemistry.

6. Conclusions[26] We have identified two fundamentally differenttypes of dike propagation behavior that may be ex-pected at mid-ocean ridge volcanoes: one that we in-terpret here as typical for the region that is above ornear the primary region of magma production and stor-age and one that we interpret as typical of the distalportions of rift zones. All types of dikes discussed hereare steep and parallel to the ridge axis. Near a sourceof magmatic upwelling, sheeted dikes intrude verticallyupward and intrusive directions shoal in a radial fash-ion as dikes intrude farther out from this magmatic cen-ter. These ridge-parallel vertical sheets with radial in-trusive angles may form unidirectional sheets as illus-trated in Figure 6, or they may represent continuoussheets that propagate radially outward, perhaps feed-ing fissure eruptions. In either case, the focus of intru-sive directions points toward a central intrusive zone,and intrusive directions may be used to infer the loca-tion of a magma chamber [Knight and Walker, 1988].Distant types of dike intrusions are dominated by lat-eral and vertical intrusive directions. Horizontal dikeintrusive directions maintain the main magma supplyfrom the central magma chamber, and vertical direc-tions supply rift zone eruptions with magma from thehorizontal feeders (Figure 6).

[27] While all these conclusions display a high degreeof internal consistency, and suggest a rather simplemodel for the propagation of dikes in volcanic riftzones, we wish to reiterate some of the weaknesses ofthis study. In particular, our uncertainties about the ac-tual paleohorizontal weaken our arguments, and it isobvious that our interpretations are strongly linked toa wide body of other information that comes from ob-servations on active volcanoes, in particular, Kilauea,







Krafla, and, most recently, the Juan de Fuca Ridge.However, it also demonstrates the power ofmultidisciplinary investigations, where employment ofseveral different Earth science approaches together canbe successfully used to enhance our understanding ofhow the Earth works. In our particular case, the mar-riage of geochemistry with paleomagnetism provedsuccessful in providing a new look at intrusive processesat constructive plate margins. In fact, it is quite obvi-ous that the integrated results provide significantlystronger insights than the sum of the individual dataset.

Acknowledgments[28] This is a contribution of the Netherlands Research Schoolfor Sedimentary Geology, and we acknowledge the generousfunding of our field efforts through the Faculteit voorAardwetenschappen of the Free University (for all participantsexcept L.T. and J.S.G.). M.-A. Broekema supervised much ofthe analytical work in the XRF laboratory, and E. Burke su-pervised the microprobe work. We also acknowledge the closecooperation with R. Varga, who has been a great contributorto our joint AMS Cyprus effort. We also acknowledge the lo-gistical support by the Geological Survey Department, in par-ticular, from George Constantinou and Costas Xenophontas,and the Cyprus—American Archeological Research Institute(CAARI). L.T. acknowledges funding from the National Sci-ence Foundation. We acknowledge reviews by J. Karson, J.Phipps-Morgan, N. Sleep, and two anonymous reviewers, whosubstantially improved this manuscript.

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Appendix. Data Tables

Edec Einc Erake Wdec Winc Wrake

TR - 1 35.0122 33.1794 Klirou Bridge 1D-W 157.4 -17.7 -19.1TR - 2 35.0122 33.1794 Klirou Bridge 1L-W 353.8 14.5 14.6TR - 3 35.0122 33.1794 Klirou Bridge 1L-E 172.3 77 77.1TR - 5 35.0122 33.1794 Klirou Bridge 2D-B 2.5 -29 -29 20.5 -11.9 -12.7TR - 6 35.0122 33.1794 Klirou Bridge 1L-E 0.2 20.9 20.9TR - 7 35.0383 33.1533 Kamara Pot 2L 349 80.3 80.5 44.1 82.3 84.5TR - 8 35.0383 33.1533 Kamara Pot 2L 351.1 47.9 48.2 356.5 51 51.1TR - 9 34.9961 32.9042 Kakopetria 2D-A 342.2 -22.3 -23.3 17.8 -25.6 -26.7TR - 11 34.9961 32.9042 Kakopetria 1L-W 1.6 0.7 0.7TR - 12 34.9961 32.9042 Kakopetria 1L-E 2.2 9.2 9.2TR - 13 34.9961 32.9042 Kakopetria 1D-E 219.7 -72 -76TR - 17 35.0717 32.9383 Mandres 1D-W 39.5 -71.6 -75.6TR - 18 35.0717 32.9383 Mandres 2D-A 271.7 -67.8 -89.3 152.6 -75.4 -77TR - 19 35.0717 32.9383 Mandres 1D-W 53.6 80.1 84.1TR - 21 35.0717 32.9383 Mandres 2D-A 269.6 -84.2 -90 117.5 -71.6 -81.3TR - 22 35.0717 32.9383 Mandres 1L-E 166.1 79.1 79.4TR - 25 34.9214 33.1908 Kionia 1D-E 191.6 -57.8 -58.3TR - 27 34.9214 33.1908 Kionia 1D-E 221.2 -34.2 -42.1TR - 28 34.9214 33.1908 Kionia 2D-B-STR - 29 34.9214 33.1908 Kionia 1D-W 152.5 -46.1 -49.5TR - 30 34.9214 33.1908 Kionia 2D-B 194.9 33.4 34.3 167.8 49.8 50.4TR - 32 34.9214 33.1908 Kionia 2D-A 200.5 -51.4 -53.2 157.3 -48.4 -50.7TR - 33 34.9214 33.1908 Kionia 1D-W 84.2 -67.7 -87.6TR - 36 35.0414 32.9056 Erikhou 2D-B 226.9 58.7 67.4 173.6 -84 -84TR - 38 35.0414 32.9056 Erikhou 2D-A 169.3 -70.1 -70.4 156.8 -56.9 -59.1TR - 40 34.9214 33.1908 Kionia 1L-E 8 53.4 53.7TR - 42 34.9961 33.2447 George's CYN 1D-E 196.8 -2.2 -2.3TR - 44 34.9833 33.2450 Onouphrios 1D-E 330.9 -72.1 -74.2TR - 45 34.9833 33.2450 Onouphrios 1D-E 283.9 -77.6 -87TR - 46 34.9214 33.1908 Kionia 2D-A 207.6 -72.9 -74.7 162.1 -58 -59.3TR - 47 34.9833 33.2450 Onouphrios 1D-W 243.6 -62.7 -77.1TR - 49 34.9833 33.2450 Onouphrios 2D-B 329.4 -77.6 -79.3 38.8 -83.8 -85.2TR - 50 34.9833 33.2450 Onouphrios 1D-E 191.1 -35.3 -35.8TR - 52 34.9833 33.2450 Onouphrios 1D-E 197.2 -60.2 -61.3

Western MarginEastern MarginLAT ˚N LONG ˚E

Location Data ClassSample

Table 1. Sample Numbers, Locations, Paleomagnetic Data Classification, and AMS Data of Dikes From the Troodos Ophiolite, Cyprus










Table 1. (con't.) Sample Numbers, Locations, Paleomagnetic Data Classification, and AMS Data of Dikes From the Troodos Ophiolite, Cyprus

TR - 53 34.9833 33.2450 Onouphrios 1D-E 306.6 -75.9 -81.5TR - 54 34.9833 33.2450 Onouphrios 1D-W 20.8 55.2 57TR - 55 34.9833 33.2450 Onouphrios 2D-A 228.6 -64.3 -72.3 161.1 -61.9 -63.2TR - 56 34.9833 33.2450 Onouphrios 1D-E 231.9 -63.1 -72.6TR - 57 34.9833 33.2450 Onouphrios 1D-E 210.7 -14.4 -16.6TR - 58 34.9833 33.2450 Onouphrios 2D-A 266.7 -75.1 -89.1 154.6 -61.4 -63.8TR - 59 34.9833 33.2450 Onouphrios 2D-I-STR- 100 34.9870 34.2341 Kampia Mine 2D-B 170.7 49.7 50.1 171.2 49.5 49.8TR- 101 34.9869 34.2341 Kampia Mine 1L-E 176.5 65.1 65.1TR- 103 34.9868 34.2339 Kampia Mine 2D-B 357.9 -58.6 -58.6 11.9 -61 -61.5TR- 104 34.9856 34.2305 Kampia Mine 1L-W 206.4 66.5 68.7TR- 106 34.9856 34.2304 Kampia Mine 2D-A 213.2 -77.4 -79.4 113.8 -55.9 -74.7TR- 107 34.9856 34.2304 Kampia Mine 2D-A 186.5 -2.4 -2.4 150.5 -18.9 -21.5TR- 108 34.9829 33.8993 Kampia Mine 1D-W 11.3 -0.3 -0.3TR- 110 34.9864 34.2303 Kampia Mine 1D-W 353.7 -16.1 -16.2TR- 111 34.9859 34.2299 Kampia Mine 2D-B 315.5 -82.2 -84.4 62.5 -67.5 -79.2TR- 114 34.9851 34.2285 Kampia Mine 1D-W 12.3 -40.6 -41.3TR- 115 34.9851 34.2285 Kampia Mine 1D-W 114.6 -68.8 -80.8TR- 133 34.9898 34.2265 Kampia Mine 1D-W 163.7.4 -61.6 0.4TR- 134 34.9895 34.2269 Kampia Mine 1D-E 200.8 24.1 25.6TR- 135 34.9895 34.2269 Kampia Mine 2D-A 210.7 41.6 45.9 162.5 43 44.4TR- 136 34.9901 34.2288 Kampia Mine 1L-E 349.3 21.1 21.4TR- 137 34.9832 34.2307 Kampia Mine 1D-E 197 53.9 55.1TR- 138 34.9832 34.2308 Kampia Mine 2D-A 205.3 19.6 21.5 174.5 22.1 22.2TR- 139 34.9832 34.2308 Kampia Mine 1D-E 186.3 29.8 29.9TR- 140 34.9833 34.2310 Kampia Mine 1D-E 316.6 -82.2 -84.3TR- 141 34.9834 34.2310 Kampia Mine 1L-W 18.8 77.3 78TR- 142 34.9946 34.2383 Kampia Mine 1D-W 33.8 42.1 47.4TR- 143 34.9944 34.238 Kampia Mine 2D-B 194.4 -22.4 -23.1 173.8 -8.7 -8.8TR- 144 34.9943 34.2376 Kampia Mine 2D-A 293.4 60.5 77.3 152.8 70.3 72.3TR- 147 35.0022 34.2357 Kampia Mine 1L-W 352.1 38.3 38.6TR- 149 34.9991 34.2329 Kampia Mine 2D-B-STR- 150 34.9919 33.2492 Onouphrios 1L-W 28.1 63.2 66TR- 153 34.9919 33.2492 Onouphrios 1L-E 7.1 5.5 5.5TR- 154 34.9919 33.2492 Onouphrios 2D-B 237.1 -46.5 -62.7 184.2 -61.5 -61.6TR- 155 34.9919 33.2492 Onouphrios 1L-E 110.2 65.6 81.1TR- 156 34.9919 33.2492 Onouphrios 2L 12.1 68.4 68.8 357.9 77 77TR- 157 34.9919 33.2492 Onouphrios 1L-E 354 38.6 38.8TR- 158 34.9919 33.2492 Onouphrios 2D-A 267.7 -67.5 -89 163.9 -78.6 -79TR- 159 34.9919 33.2492 Onouphrios 2D-B 195.5 -30.6 -31.5 173.3 -10.7 -10.8TR- 162 35.0006 34.2340 Kampia Mine 1D-W 24 -70.6 -72.2TR- 163 34.9997 34.2329 Kampia Mine 1L-E 329.6 64.9 68TR- 164 34.9997 34.2329 Kampia Mine 1D-E 299 -59.5 -74.1TR- 165 34.9997 34.2311 Kampia Mine 1D-E 203.6 -10.3 -11.2TR- 166 34.9906 34.2356 Kampia Mine 1D-E 328.5 -66.9 -70TR- 167 34.9907 34.2357 Kampia Mine 1D-E 192.3 -72.7 -73.1TR- 168 34.9938 34.2365 Kampia Mine 1L-W 45.8 71.1 76.6TR- 170 34.9951 34.2366 Kampia Mine 1D-E 216.9 -72.8 -76.1TR- 171 35.0032 34.2378 Kampia Mine 1L-W 162.2 25.8 26.9TR- 174 34.9914 34.2323 Kampia Mine 1D-W 122.9 -73.4 -80.8TR- 175 34.9910 34.2321 Kampia Mine 2D-A 196.6 -58.8 -59.9 169.1 -68.2 -68.6TR- 176 34.9909 34.2322 Kampia Mine 2D-A 210.5 -40.7 -45 152.8 -63.9 -66.5TR- 177 34.9912 34.2326 Kampia Mine 2D-B 190.8 -32.3 -32.8 168.3 -27.3 -27.8











TR- 178 34.9912 34.2327 Kampia Mine 1D-E 186.3 20.5 20.6 999TR- 179 34.9912 34.2330 Kampia Mine 1D-W 171.1 24.1 24.4TR- 180 34.9906 34.2320 Kampia Mine 2D-A 212.1 -62 -65.8 140.1 -71.1 -75.3TR- 181 34.9944 34.2369 Kampia Mine 1D-E 189.9 -46.5 -46.9TR- 182 34.9945 34.2370 Kampia Mine 1D-E 194 -13.9 -14.3TR- 189 34.9895 34.2318 Kampia Mine 1D-E 344.8 -64.4 -65.2TR- 190 34.9894 34.2328 Kampia Mine 1L-E 265 75.3 88.7TR- 203 34.9943 34.2376 Kampia Mine 2D-B 187.3 52.5 52.7 148.8 45.5 50TR- 204 34.9943 34.2376 Kampia Mine 2D-B 213.5 49.1 54.2 165.6 52.9 53.8TR- 205 35.0007 34.2374 Kampia Mine 1D-E 241.5 66 78TR- 206 35.0033 34.2357 Kampia Mine 2D-B 210.4 1.7 2 171.7 0.2 0.2TR- 207 35.0033 34.2359 Kampia Mine 2D-A 203 -24.6 -26.4 157.8 -4.1 -4.4TR- 209 35.0030 34.2371 Kampia Mine 2D-B 212.3 -40.2 -45 167.4 -42.6 -43.3TR- 210 34.9992 34.2328 Kampia Mine 1D-E 22.5 3.7 4TR- 211 34.9971 34.2325 Kampia Mine 1L-W 999 999 178.7 57.1 57.1TR- 212 34.9971 34.2325 Kampia Mine 1D-E 184.3 -34.3 -34.4TR- 214 34.9950 34.2317 Kampia Mine 2L 114.5 60.7 76.9 128.1 60.7 70.9TR- 215 34.9953 34.2317 Kampia Mine 2L-STR- 216 34.9952 34.2317 Kampia Mine 2D-A 328.6 -74.2 -76.4 48.2 -69.9 -76.3TR- 221 34.9783 33.2420 Onouphrious 2D-A 198.5 5.4 5.7 160.1 -12.4 -13.2TR- 222 34.9780 33.2421 Onouphrious 2D-A 338.8 -53 -54.9 114.3 -64.5 -78.9TR- 223 34.9779 33.2420 Onouphrious 1L-E 162.6 39 40.3TR- 224 34.9778 33.2421 Onouphrious 2D-A 313.6 -74.8 -79.4 86.2 -82.4 -89.5TR- 225 34.9760 33.2409 Onouphrious 2D-A 349.3 -21.9 -22.2 6.4 -30.4 -30.6TR- 226 34.9759 33.2408 Onouphrious 1D-W 160.7 59.2 60.6TR- 228 34.9744 33.2400 Onouphrious 2D-B 343.6 -72.2 -72.9 81.7 -77.7 -88.2TR- 229 34.9742 33.2400 Onouphrious 2L 170.6 16.8 17 174.2 43.8 43.9TR- 230 34.9703 33.2383 Onouphrious 2D-B 141.1 -79.2 -81.6 117.9 -73 -81.9TR- 231 34.9688 33.2352 Onouphrious 2D-A 271.3 78 89.7 160.3 73.1 74TR- 232 34.9686 33.2351 Onouphrious 2D-B 196.3 -73.4 -74 122.6 -83.7 -86.6TR- 234 34.9682 33.2347 Onouphrious 1D-E 188.3 -37.8 -38.1TR- 235 34.9681 33.2346 Onouphrious 2D-A 213.4 -65.1 -68.8 114.9 -73 -82.7TR- 236 34.9651 33.2349 Onouphrious 2D-A 203.8 -65.5 -67.4 114.1 -74.8 -83.7TR- 237 34.9631 33.2347 Onouphrious 2D-B 185.8 -28.3 -28.4 155.8 -33.4 -35.9TR- 238 34.9619 33.2346 Onouphrious 1D-W 165 -36.8 -37.8TR- 239 34.9596 33.2326 Onouphrious 1D-E 197.4 -78.6 -79.1TR- 240 34.9596 33.2325 Onouphrious 1L-W 176.8 61.6 61.6TR- 241 34.9598 33.2299 Onouphrious 1D-W 53.8 -71.6 -78.9TR- 242 34.9601 33.2281 Onouphrious 2D-B 272 -70.1 -89.3 119.6 -77.5 -83.8TR- 243 34.9602 33.2279 Onouphrious 2L 206.7 72.8 74.5 267.2 70.7 89TR- 244 34.9601 33.2278 Onouphrious 2L 33.8 87 87.5 336 76.1 77.3TR- 245 34.9795 33.2013 Pedhieos 2D-A 343.6 -5.5 -5.7 11.4 -10.2 -10.4TR- 246 34.9783 33.2015 Pedhieos 2D-B 356.6 -43.2 -43.3 32 -48 -52.6TR- 247 34.9777 33.2013 Pedhieos XTR- 248 34.9776 33.2014 Pedhieos 2D-A 186.5 -46.1 -46.3 156.6 -69.6 -71.2TR- 249 34.9774 33.2013 Pedhieos 2D-A 339.2 -66.2 -67.6 163.2 -80.2 -80.6TR- 250 34.9768 33.2013 Pedhieos XTR- 251 34.9763 33.2014 Pedhieos 2D-A 199.8 -68.3 -69.5 157 -52.4 -54.7TR- 252 34.9753 33.2016 Pedhieos 2L 343.5 4 4.2 341.6 -16.2 -17TR- 253 34.9752 33.2017 Pedhieos 2D-B 350 -33.6 -34 31 -51.5 -55.7TR- 254 34.9739 33.2025 Pedhieos 2D-A 238.5 -44 -61.6 35.4 -50.3 -55.9TR- 255 34.9720 33.2027 Pedhieos 2L 176.8 64.6 64.6 202 68.1 69.6

TR- 256 34.9718 33.2026 Pedhieos 1D-W 18.5 -27.3 -28.6











TR- 257 34.9716 33.2027 Pedhieos 1D-W 167 -8.4 -8.6TR- 258 34.9683 33.2024 Pedhieos 1D-W 148.8 -59.8 -63.5TR- 260 34.9656 33.2028 Pedhieos 2D-A 186.4 -36.2 -36.4 166 -27.6 -28.3TR- 262 34.9654 33.203 Pedhieos 2D-B 205.5 -36.6 -39.4 173.6 -36.6 -36.8TR- 264 34.9610 33.2034 Pedhieos 2D-B 205.4 -34.8 -37.6 178.1 -38.8 -38.8TR- 265 34.9608 33.2034 Pedhieos 2D-B 342.8 -67.5 -68.4 29.1 -55.2 -58.7TR- 266 34.9601 33.2039 Pedhieos 1D-W 173.3 -0.8 -0.8TR- 267 34.9577 33.2018 Pedhieos 2D-B 314.2 -52.8 -62.1 359 -57.3 -57.3TR- 268 34.9553 33.2008 Pedhieos 2D-A 246.3 -73.6 -83.3 147.5 -73.8 -76.2TR- 269 34.9524 33.1995 Pedhieos 2D-B 201.4 31.1 32.9 339.9 27 28.5TR- 271 34.9291 34.4669 Kionia Road 2D-A 216.1 -63.1 -67.7 158 -72.2 -73.4TR- 272 34.9291 34.5093 Kionia Road 1D-E 26.2 -36.8 -39.8TR- 273 34.9279 34.5843 Kionia Road 1D-W 141.3 -70.2 -74.3TR- 274 34.9276 34.5679 Kionia Road 2D-B 184.8 -30.5 -30.6 159.3 -37.4 -39.3TR- 275 34.9300 34.5700 Kionia Road 1L-E 10.3 43.5 44TR- 300 34.9610 33.2242 Onouphrious 2D-B 261.7 -82.5 -88.9 2.4 -80.4 -80.4TR- 301 34.9608 33.224 Onouphrious 2D-A 275.4 -65.5 -87.5 71.7 -75.8 -85.5TR- 303 34.9602 33.2218 Onouphrious 1L-E 355.8 14.5 14.5TR- 304 34.9602 33.2215 Onouphrious 2L 22.7 75.8 76.9 354.6 80.5 80.5TR- 305 34.9597 33.2213 Onouphrious 2D-A 347.4 -73.2 -73.6 35.4 -74.6 -77.3TR- 306 34.9600 33.2195 Onouphrious 2L 102.8 82 88.2 27.5 72.6 74.5TR- 309 34.9540 33.2132 Onouphrious 1D-E 191.1 -21.2 -21.6TR- 315 34.9378 33.2055 Onouphrious 1D-E 337.6 52.2 54.4TR- 316 34.9473 33.1958 Pedhieos 1D-E 195.3 -33.6 -34.6TR- 317 34.9470 33.1950 Pedhieos 1D-E 202.8 -38.9 -41.2TR- 318 34.9465 33.1937 Pedhieos 2D-A 203.1 -56.4 -58.6 152.4 -47.9 -51.3TR- 319 34.9460 33.1920 Pedhieos 2D-B 11.1 -80.3 -80.5 93.8 -79.6 -89.3TR- 320 34.9443 33.1883 Pedhieos 1D-W 332.7 -2.5 -2.8TR - 322 34.9445 33.1875 Pedhieos 1D-W 167.4 -25.1 -25.6TR - 324 34.9445 33.1873 Pedhieos 2D-A 199.3 -38.7 -40.3 172.2 -42.3 -42.6TR - 325 34.9445 33.1872 Pedhieos 1D-W 154.1 -65 -67.2TR - 326 34.9445 33.1868 Pedhieos 2D-B 198.9 -54.6 -56.1 160.7 -31.6 -33.1TR - 327 34.9608 33.1865 Pedhieos 2D-I-S 999TR - 328 34.9615 33.1852 Pedhieos 2D-A 187.7 -42.1 -42.4 165.9 -19.1 -19.6TR - 329 34.9602 33.1813 Pedhieos 2D-A 285.3 -65.4 -83.1 13.3 -70.2 -70.7TR - 332 34.9573 33.1803 Pedhieos 2D-A 191.1 1.5 1.5 172.8 -0.9 -0.9TR - 333 34.9563 33.1800 Pedhieos 2D-A 195.5 -55 -56 163 -41.5 -42.8TR - 334 34.9562 33.1800 Pedhieos 2D-B 195.2 -60.2 -61.1 168.5 -58.6 -59.1TR - 335 34.9553 33.1800 Pedhieos 2D-A 198.9 -15.3 -16.1 156 -19.7 -21.4TR - 336 34.9548 33.1777 Pedhieos 2D-B 199 -47.1 -48.7 154.6 -65.9 -68TR - 337 34.9547 33.1775 Pedhieos 2D-B 179.6 -7.7 -7.7 152.4 -16.2 -18.2TR - 340 34.9379 34.4510 Onouphrious 2D-A 191.9 -25.3 -25.8 161.5 -22.3 -23.4TR - 341 34.9379 34.4684 Onouphrious 1D-E 192 -10.9 -11.1TR - 342 34.9380 34.4720 Onouphrious 2L 204.3 50.2 52.8 213.3 45.1 50.2TR - 344 34.9382 34.5064 Onouphrious 2D-A 261.9 -78.6 63.3 -69.6 -80.5TR - 345 34.9373 34.6078 Onouphrious 2D-A 196 -24.1 -25 166.4 -36.7 -37.5TR - 346 34.9363 34.6602 Onouphrious 2D-A 350.4 -55.2 -55.6 18.6 -56.9 -58.3TR - 347 34.9347 34.6660 Onouphrious 2D-B 313.7 -68.3 -74.6 4.2 -54.8 -54.9

TR - 348 34.9327 34.6530 Onouphrious 2D-A 201.1 8.9 9.5 154.9 1 1.1

Notes: Data Class gives the classification of the AMS data following Tauxe et al. [1998]. AMS Eigenvector data are given for Easter and Western Margins including declination (Edec, Wdec) and inclination (Wdec Winc) and the

rake in the dike plane (Wrake, Erake). The latter are interpreted as the dike propagation directions in this paper.







Table 2a. Major and Trace Element Analysis of Bulk Rock Samples From the Troodos Ophiolite, Cyprus

Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 BaO LOI Sum Sr Zr Y V Cr Co Ni Cu Zn

TR - 100 56.16 1.26 15.11 11.65 0.16 5.00 5.09 2.97 0.32 0.11 0.01 2.4 97.84 91 78 36 306 35 36 9 47 110

TR - 103 54.90 1.27 14.15 12.31 0.25 5.92 3.86 3.06 0.46 0.10 n.d. 2.8 96.28 90 65 32 401 28 43 9 40 151

TR - 106 52.86 0.94 15.02 10.96 0.18 7.13 3.63 4.90 0.37 0.07 n.d. 3.3 96.06 93 46 23 301 28 39 13 49 95

TR - 107 55.83 1.27 14.39 11.35 0.16 5.11 3.49 4.82 0.11 0.12 n.d. 3.0 96.65 102 70 35 253 24 34 5 11 97

TR - 110 55.47 1.33 14.84 12.05 0.13 4.42 1.90 5.99 0.39 0.10 n.d. 2.5 96.62 20 66 31 374 27 41 10 110 86

TR - 111 60.10 1.22 14.52 10.42 0.11 3.81 2.28 5.76 0.07 0.13 n.d. 1.9 98.42 83 81 41 163 15 28 2 2 149

TR - 134 51.90 1.02 15.86 11.69 0.25 8.05 5.35 2.47 0.53 0.08 0.01 3.5 97.21 75 46 25 336 33 42 21 37 189

TR - 135 49.48 1.16 16.11 13.83 0.35 7.50 2.02 5.95 0.05 0.09 n.d. 3.9 96.54 77 60 29 238 34 45 24 36 177

TR - 136 52.89 1.33 14.75 12.74 0.27 7.10 2.95 4.69 0.07 0.10 n.d. 3.0 96.89 84 66 30 405 25 43 12 43 102

TR - 138 55.65 1.27 14.29 12.36 0.15 6.45 1.69 4.72 0.03 0.10 n.d. 3.1 96.71 47 63 31 356 25 46 7 16 67

TR - 139 55.29 1.20 14.17 12.30 0.12 5.09 2.18 5.20 0.39 0.09 n.d. 4.0 96.03 62 58 30 362 24 39 13 51 59

TR - 140 54.74 1.14 13.32 12.76 0.18 5.46 3.80 5.23 0.59 0.08 n.d. 2.4 97.30 32 55 28 398 29 40 16 n.d. 53

TR - 141 54.54 1.12 15.35 11.12 0.15 5.69 3.11 6.06 0.32 0.09 n.d. 2.5 97.55 40 59 29 319 29 36 15 n.d. 73

TR - 143 58.11 1.22 15.99 8.97 0.12 3.12 6.56 3.12 0.23 0.10 0.01 1.4 97.55 95 59 25 329 27 27 10 50 110

TR - 144 57.38 1.06 16.14 9.16 0.09 4.04 7.60 2.55 0.14 0.08 0.01 1.6 98.25 87 46 24 349 38 33 21 96 84

TR - 144 57.97 1.07 16.33 9.24 0.09 4.09 7.66 2.57 0.14 0.08 0.01 1.4 99.25 86 46 24 351 39 33 21 98 86

TR - 148 51.62 0.70 15.54 8.01 0.20 6.88 11.96 2.16 0.06 0.06 n.d. 3.2 97.19 93 33 18 251 258 38 52 37 82

TR - 148 51.46 0.70 15.53 8.08 0.20 6.89 11.95 2.16 0.07 0.05 n.d. 3.2 97.09 93 33 18 249 257 39 52 37 85

TR - 159 55.33 0.81 16.41 9.01 0.08 3.62 7.85 2.64 1.87 0.07 0.01 2.2 97.70 101 43 17 300 28 29 12 25 64

TR - 161 50.15 0.53 15.36 8.15 0.13 8.76 12.22 1.95 0.18 0.04 n.d. 3.0 97.47 91 29 15 224 439 41 122 26 63

TR - 163 65.24 1.07 13.47 7.45 0.10 1.54 5.18 3.10 1.53 0.12 0.01 1.2 98.81 82 61 30 155 35 16 4 8 84

TR - 164 52.76 0.50 15.49 8.36 0.14 8.02 10.49 1.90 0.16 0.04 n.d. 2.1 97.86 91 25 13 227 258 41 92 88 64

TR - 165 48.19 0.42 13.36 6.14 0.26 7.22 16.17 1.51 0.31 0.03 n.d. 6.8 93.61 78 20 14 226 321 37 52 56 56

TR - 167 54.00 1.29 14.18 12.81 0.19 5.83 4.41 3.74 0.31 0.10 0.01 3.1 96.87 93 64 28 418 31 42 12 31 152

TR - 169 62.63 1.25 15.81 7.00 0.12 2.64 5.03 4.25 0.30 0.16 0.01 1.1 99.20 109 101 42 118 24 23 3 15 99

TR - 170 57.49 1.39 15.47 10.08 0.15 3.66 7.05 3.17 0.38 0.10 0.01 1.0 98.95 102 66 26 446 25 34 11 64 96

TR - 171 51.23 0.65 15.95 10.48 0.08 7.62 8.27 2.16 1.14 0.08 n.d. 2.2 97.66 86 31 17 250 200 35 36 29 66

TR - 174 62.56 1.15 14.06 8.98 0.12 2.96 5.79 2.84 0.19 0.10 n.d. 1.3 98.75 85 56 30 293 23 41 5 33 89

TR - 176 57.29 1.34 14.53 11.15 0.11 4.10 6.15 3.00 0.18 0.11 0.01 1.4 97.97 93 65 30 399 25 32 10 56 90

TR - 178 57.08 1.04 15.46 9.60 0.10 4.55 7.28 2.70 0.19 0.10 0.01 1.7 98.11 92 52 26 302 28 32 16 43 80

TR - 179 59.22 0.54 15.95 6.96 0.06 5.16 8.70 1.91 0.34 0.05 0.01 1.4 98.90 75 24 14 236 107 25 22 97 60

TR - 182 56.36 0.58 15.54 8.61 0.09 5.23 8.15 2.45 1.45 0.06 0.01 1.4 98.53 85 53 25 369 43 29 12 37 81

TR - 183 61.36 1.31 14.46 8.86 0.15 3.13 6.00 3.18 0.22 0.11 0.01 1.0 98.79 100 72 29 298 34 44 2 18 94

TR - 187 57.32 1.14 14.47 11.81 0.07 4.78 5.71 2.84 0.17 0.08 0.01 1.9 98.40 84 51 25 333 36 42 13 38 95

TR - 189 58.28 1.30 14.64 10.74 0.10 4.01 6.22 2.98 0.15 0.11 0.01 1.5 98.54 94 64 31 415 32 38 13 67 91

TR - 191 54.08 0.57 15.99 8.98 0.07 6.88 10.07 1.84 0.06 0.04 n.d. 1.6 98.58 69 21 14 245 104 53 56 70 42

TR - 200 55.30 1.203 14.50 12.60 0.219 5.24 3.66 4.32 0.072 0.086 0.003 2.7 97.203 100 66 30 346 58 29 13 0 116

TR - 201 55.10 1.209 13.90 12.59 0.251 4.39 6.43 3.96 0.089 0.09 0.002 3.2 98.012 87 61 30 362 68 41 14 2 95

TR - 202 55.50 1.364 15.60 12.43 0.231 3.88 4.25 5.27 0.157 0.102 0.002 1.9 98.782 115 70 33 378 47 38 11 10 98

TR - 206 53.37 0.78 15.93 10.91 0.09 5.65 6.87 2.79 1.30 0.08 n.d. 2.1 97.77 105 41 20 307 25 42 12 46 72

TR - 206 53.93 0.79 16.02 10.99 0.10 5.71 6.94 2.79 1.32 0.08 n.d. 2.2 98.67 105 41 20 307 26 43 13 46 72

TR - 207 55.88 0.57 15.42 8.54 0.09 5.21 8.04 2.45 1.44 0.06 n.d. 2.3 97.70 103 33 15 219 244 29 34 13 57

TR - 208 56.45 0.62 15.67 7.97 0.09 6.47 8.95 2.17 0.16 0.05 n.d. 1.6 98.6 95 32 15 237 147 28 42 44 47

TR - 209 52.58 0.58 16.96 7.84 0.10 5.40 11.61 2.42 1.00 0.05 0.01 1.8 98.55 92 29 14 246 329 34 80 13 60

TR - 210 55.32 1.19 14.66 8.21 0.18 3.14 9.86 3.02 0.41 0.11 n.d. 4.2 96.10 96 60 34 254 22 62 48 37 94

TR - 213 57.07 0.82 16.03 7.67 0.08 5.53 8.97 2.25 0.17 0.07 n.d. 1.5 98.66 98 40 18 266 93 32 40 64 74

TR - 214 55.71 1.04 16.89 8.85 0.09 4.87 8.77 2.63 0.11 0.08 n.d. 1.5 99.04 105 52 24 311 53 38 30 68 84

TR - 216 65.55 1.21 13.24 7.83 0.12 2.11 5.72 3.11 0.19 0.12 0.01 1.1 99.21 96 72 32 240 20 24 1 8 80

TR - 216 65.66 1.21 13.26 7.82 0.12 2.10 5.73 3.14 0.19 0.12 0.01 1.1 99.36 96 72 32 240 21 27 2 8 80

TR - 221 55.60 1.335 14.40 12.42 0.196 3.54 5.82 3.08 0.602 0.093 0.003 1.5 97.093 92 63 33 274 56 45 6 80 90

TR - 222 55.10 1.247 14.70 12.64 0.155 4.64 4.13 4.73 0.809 0.083 0.004 2.7 98.244 107 59 28 388 35 38 7 0 45

TR - 224 55.80 1.429 14.50 12.16 0.191 4.73 5.56 3.23 0.452 0.133 0.001 2.3 98.181 108 76 35 289 46 32 10 3 58

TR - 225 56.30 1.094 14.00 13.37 0.151 4.85 3.85 3.51 0.163 0.089 0.003 3.2 97.373 79 66 29 269 54 34 20 25 41

TR - 228 54.90 1.273 15.10 13.58 0.15 4.08 5.90 4.29 0.483 0.086 0.003 1.2 98.843 115 59 22 394 39 38 18 0 33

TR - 231 58.90 1.180 14.70 10.07 0.106 4.50 6.38 3.65 0.255 0.090 0.003 1.1 99.843 96 90 35 307 76 34 17 0 13

TR - 233 56.00 1.214 14.60 12.95 0.122 4.92 5.99 3.34 0.18 0.083 0.001 1.8 99.391 98 58 23 391 51 39 18 0 15TR - 235 53.80 1.272 15.40 12.15 0.138 4.74 6.77 5.28 0.085 0.094 0.001 1.2 99.731 106 65 30 441 39 38 18 0 19







Table 2a. (con't.) Major and Trace Element Analysis of Bulk Rock Samples From the Troodos Ophiolite, Cyprus

Sample SiO2 TiO2 Al2O3 Fe2O3 MnO MgO CaO Na2O K2O P2O5 BaO LOI Sum Sr Zr Y V Cr Co Ni Cu Zn

TR - 236 54.40 1.164 14.30 16.02 0.124 4.78 3.76 2.47 1.454 0.085 0.004 2.6 98.554 81 59 26 366 48 50 19 1 26TR - 237 54.90 1.348 15.00 13.15 0.147 4.18 6.54 4.41 0.069 0.105 0.001 1.2 99.861 98 72 35 391 35 36 15 11 23TR - 239 51.50 1.30 16.00 12.92 0.14 5.51 7.80 4.38 0.157 0.088 0.002 1.1 99.802 131 63 33 419 37 41 22 0 30

TR - 240 55.60 1.276 15.30 11.63 0.103 4.15 6.90 4.11 0.568 0.097 0 1.5 99.74 111 66 29 379 46 34 16 0 19

TR - 242 57.80 1.149 14.30 12.59 0.122 3.81 6.69 3.11 0.113 0.107 0.002 1.0 99.792 94 71 33 339 66 41 17 0 13

TR - 245 55.00 1.116 15.00 11.83 0.144 4.79 3.20 6.24 0.036 0.074 0.003 3.2 97.433 56 51 26 362 49 37 17 4 94

TR - 246 53.50 1.117 15.70 12.15 0.160 4.57 4.84 6.51 0.038 0.074 0 2.3 98.660 19 46 26 370 34 35 11 27 53

TR - 248 53.70 1.062 15.60 12.20 0.156 4.80 4.74 5.87 0.036 0.065 0.002 2.4 98.242 27 43 24 391 37 35 13 0 78

TR - 249 51.20 0.922 15.50 11.61 0.203 8.07 4.17 5.32 0.194 0.062 0.002 3.3 97.242 27 41 24 340 36 38 24 82 138

TR - 251 51.60 1.207 16.20 12.71 0.192 4.35 5.61 6.06 0.054 0.077 0.002 2.4 98.062 17 53 27 429 27 34 19 42 78

TR - 253 52.30 0.662 15.30 10.61 0.181 7.00 6.53 5.48 0.029 0.042 0 2.5 98.130 18 26 18 276 48 45 34 78 82

TR - 254 53.20 0.866 15.70 10.65 0.181 5.55 5.85 6.02 0.051 0.059 0.001 2.4 98.131 34 40 22 300 36 43 31 0 76

TR - 256 52.50 1.029 16.90 11.99 0.156 4.33 4.30 6.69 0.009 0.069 0.001 2.3 97.981 43 46 25 326 30 41 18 38 60

TR - 258 52.00 0.797 15.60 10.25 0.171 7.06 6.86 5.09 0.022 0.050 0.002 2.9 97.902 20 61 30 306 107 37 18 0 53

TR - 259 52.50 1.47 15.50 13.76 0.147 3.80 5.01 6.37 0.052 0.094 0.002 2.2 98.702 30 42 22 479 38 43 27 0 34

TR - 260 52.50 0.95 15.40 10.95 0.143 5.65 6.41 5.75 0.033 0.059 0 2.3 97.840 128 43 24 325 56 46 26 1 31

TR - 262 55.00 0.925 14.30 10.93 0.162 5.72 6.47 5.39 0.209 0.063 0.003 1.5 99.173 18 51 25 323 58 43 36 0 69

TR - 264 50.30 0.911 16.00 12.12 0.173 6.56 6.30 5.20 0.028 0.072 0.002 3.2 97.662 75 36 20 293 41 42 32 0 57

TR - 265 51.10 0.751 16.40 10.39 0.177 6.26 7.60 4.92 0.067 0.050 0.002 3.1 97.722 78 51 24 305 62 37 46 11 50

TR - 266 53.10 0.722 15.90 9.47 0.184 6.34 6.62 5.72 0.039 0.072 0.002 2.5 98.162 14 41 22 243 71 37 42 0 47

TR - 267 49.70 0.857 16.20 10.18 0.165 6.11 10.31 4.23 0.011 0.057 0.002 3.2 97.832 31 34 19 298 59 34 44 12 45

TR - 269 51.20 1.054 14.90 11.64 0.158 5.54 9.76 3.25 0.027 0.069 0 3.2 97.600 52 50 25 342 55 43 26 4 56

TR - 271 51.20 1.064 15.10 10.35 0.145 3.85 13.09 1.59 0.019 0.082 0 3.6 96.490 16 57 26 387 54 38 21 377 55

TR - 274 54.40 1.057 14.60 11.81 0.192 4.72 7.10 3.91 0.190 0.085 0.004 2.3 98.074 113 60 29 329 71 39 25 1 45

TR - 300 57.60 1.199 14.30 12.37 0.155 3.88 6.58 3.37 0.089 0.088 0.003 1.1 99.643 96 82 35 390 51 37 15 2 14

TR - 301 55.40 1.315 14.60 12.59 0.314 4.45 6.34 4.73 0.066 0.096 0 1.2 99.910 116 68 30 407 42 44 13 0 21

TR - 305 52.40 1.445 16.00 12.76 0.072 4.69 5.80 4.86 0.135 0.112 0.003 2.6 98.283 127 76 33 443 34 36 12 0 10

TR - 307 52.20 1.388 15.30 11.73 0.142 4.23 6.68 4.32 0.155 0.098 0.003 4.5 96.253 65 69 30 411 23 38 15 0 34

TR - 318 53.40 1.012 15.30 11.69 0.161 4.74 7.45 5.19 0.086 0.067 0.001 1.6 99.101 80 45 24 372 32 41 21 14 29

TR - 324 53.10 0.848 14.90 10.11 0.145 5.48 8.94 3.43 0.094 0.049 0.001 3.6 97.101 95 32 21 318 64 39 37 4 38

TR - 332 51.80 0.558 15.70 10.01 0.278 6.31 11.93 1.39 0.208 0.039 0.003 2.5 98.233 199 26 16 353 117 32 43 21 48

TR - 333 52.30 1.097 15.30 13.38 0.165 6.95 5.65 2.93 0.101 0.070 0.001 2.7 97.951 80 44 25 362 52 49 24 0 32

TR - 335 50.80 0.759 17.70 10.34 0.221 7.57 6.86 3.58 0.344 0.051 0.003 2.8 98.223 98 35 19 254 106 45 44 38 48

TR - 336 51.30 1.10 15.10 12.96 0.134 7.61 6.55 2.55 0.734 0.066 0.002 2.8 98.102 80 42 26 356 44 45 31 12 24

TR - 340 57.00 0.96 15.20 10.13 0.127 3.61 7.11 4.81 0.049 0.079 0.001 2.0 99.081 71 55 27 300 67 32 23 0 25

TR - 344 51.80 1.06 16.40 11.28 0.160 5.15 7.88 4.32 0.028 0.080 0.002 3.0 98.162 54 56 27 326 40 38 24 50 85

TR - 345 55.10 0.74 14.80 9.67 0.167 5.67 7.02 4.37 0.041 0.065 0.001 3.3 97.651 78 40 22 239 51 34 28 53 67

TR - 346 50.00 0.51 17.30 9.38 0.158 6.79 9.61 4.12 0.011 0.032 0.001 3.5 97.911 21 20 15 258 86 36 51 56 62

TR - 347 53.70 0.45 15.80 9.63 0.164 7.17 6.10 5.50 0.080 0.027 0.001 2.7 98.621 79 19 12 237 89 39 44 76 69

TR - 348 55.50 0.99 15.00 10.07 0.188 5.38 7.03 5.36 0.127 0.084 0.002 1.5 99.732 133 62 26 256 58 37 35 7 26

Standard Data (sums corrected for LOI)BHVO 1 49.69 2.75 13.65 12.32 0.171 7.25 11.44 2.28 0.524 0.269 0.013 n.d. 100.360 384 169 26 n.d. n.d. n.d. n.d. n.d. n.d.

BHVO 1 49.60 2.74 13.60 12.32 0.171 7.16 11.46 2.29 0.522 0.264 0.016 n.d. 100.140 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d.

G2 69.23 0.49 15.35 2.64 0.033 0.73 1.92 4.06 4.480 0.131 0.209 n.d. 99.270 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d.

JG 1 (1) 71.77 0.266 14.13 2.087 0.063 0.73 2.163 3.34 3.982 0.088 0.053 n.d. 98.670 185 105 32 25 68 2 8.6 1 41

JG 1 (2) n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 186 102 32 n.d. n.d. n.d. n.d. n.d. n.d.

JB 1 (1) 52.16 1.29 14.47 8.956 0.152 7.73 9.34 2.76 1.419 0.255 0.056 n.d. 98.580 444 140 24 209 482 37 135 56 86

JB 1 (2) n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 442 136 24 n.d. n.d. n.d. n.d. n.d. n.d.

SY - 2 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 270 278 137 n.d. n.d. n.d. 12 7 254

JA 2 (1) n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 246 115 18 n.d. n.d. n.d. 129 28 66

JA 2 (2) n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 246 118 19 n.d. n.d. n.d. n.d. n.d. n.d.

JF 1 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 162 38 5.8 n.d. n.d. n.d. 2.8 1 3.4

JG 1a n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 182 114 33 n.d. n.d. n.d. 8 0 35JG 2 n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. n.d. 17 101 90 n.d. n.d. n.d. 5.6 0 12

All analyses were performed by XRF using fused beads for major elements and pressed powder pellets for trace elements (using techniques of Verdumen and Broekema-Roomer [1994]).







Table 2b. Microprobe Analyses of Glassy Dike Margins From the Troodos Ophiolite, Cyprus

Sample SiO2 TiO2 Al2O3 FeO MnO MgO CaO Na2O K2O SO3 Cl Total

TR - 143 56.89 1.12 13.96 10.67 0.16 2.73 7.32 2.58 0.29 0.07 0.09 95.88TR - 143 56.34 1.13 13.89 10.22 0.16 2.67 6.97 2.18 0.27 0.08 0.09 94.01TR - 144 55.62 0.99 14.22 10.30 0.18 3.27 8.11 2.37 0.22 0.06 0.07 95.31TR - 144 55.56 1.00 14.19 10.23 0.15 3.20 7.89 2.07 0.21 0.07 0.09 94.67TR - 145 54.19 0.53 16.32 6.92 0.11 6.02 10.73 2.04 0.17 0.06 0.06 97.15TR - 146 55.69 0.56 15.51 7.36 0.14 5.60 9.55 2.52 0.27 0.07 0.10 97.35TR - 147 54.10 0.64 16.25 7.66 0.14 6.19 10.43 2.08 0.16 0.06 0.04 97.74TR - 148 53.47 0.76 15.92 8.42 0.18 5.73 10.37 2.33 0.18 0.15 0.04 97.53TR - 149 52.56 0.74 15.80 8.56 0.16 5.94 10.28 1.82 0.19 0.16 0.04 96.24TR - 149 52.42 0.73 15.77 8.32 0.17 5.96 10.36 1.97 0.18 0.17 0.04 96.07TR - 159 56.44 0.77 15.57 8.55 0.16 4.39 7.04 5.47 0.77 0.02 0.05 99.20TR - 160 53.78 0.64 16.26 7.75 0.16 6.19 10.4 2.25 0.16 0.06 0.04 97.55TR - 161 55.79 0.58 15.49 7.46 0.12 5.53 9.55 2.50 0.28 0.04 0.09 97.41TR - 165 58.05 1.16 14.14 9.13 0.16 2.12 6.07 3.14 0.27 0.08 0.23 94.39TR - 169 53.72 1.31 14.48 11.54 0.18 3.51 7.81 2.76 0.19 0.10 0.11 95.71TR - 169 53.87 1.29 14.47 11.36 0.17 3.57 7.83 2.48 0.19 0.12 0.11 95.46TR - 170 55.08 1.31 14.55 10.33 0.17 2.87 7.17 3.01 0.24 0.08 0.11 94.9TR - 171 53.85 0.66 15.94 8.01 0.15 5.86 10.12 1.80 0.21 0.07 0.04 96.71TR - 174 54.76 1.19 13.84 10.09 0.16 2.74 7.15 2.68 0.25 0.07 0.09 93.01TR - 176 51.59 1.26 13.77 10.03 0.15 3.20 7.19 2.79 0.19 0.10 0.12 90.39TR - 178 52.96 1.01 15.12 9.97 0.17 4.72 8.92 2.31 0.18 0.11 0.05 95.51TR - 179 53.60 0.54 15.88 8.37 0.15 5.73 10.13 1.99 0.23 0.03 0.06 96.70TR - 181 58.66 1.06 15.44 9.88 0.18 2.37 7.11 3.64 0.20 0.04 0.05 98.62TR - 182 51.90 0.60 15.22 9.18 0.16 6.07 10.30 1.24 0.16 0.08 0.03 94.92TR - 183 54.00 1.25 14.99 11.00 0.18 4.33 8.61 2.90 0.18 0.10 0.09 97.64TR - 185 53.64 1.04 15.28 10.08 0.18 5.00 9.30 2.52 0.17 0.09 0.05 97.36TR - 190 53.24 1.06 14.67 10.10 0.15 4.45 8.16 2.45 0.18 0.10 0.06 94.56TR - 190 53.89 1.39 14.12 11.50 0.17 3.36 7.54 3.09 0.20 0.11 0.11 95.48TR - 205 54.11 0.65 18.0 7.39 0.10 5.20 8.58 4.59 0.38 0.01 0.03 99.05TR - 206 55.45 0.76 15.36 10.08 0.17 4.33 8.93 2.43 0.26 0.02 0.06 97.84TR - 207 55.70 0.57 15.51 7.42 0.12 5.71 9.53 2.52 0.26 0.04 0.09 97.46TR - 208 53.71 0.66 16.19 7.68 0.13 6.11 10.35 2.22 0.16 0.04 0.04 97.28TR - 210 54.70 0.71 15.95 8.71 0.16 5.14 9.51 2.35 0.26 0.07 0.05 97.61TR - 216 56.73 1.56 14.12 10.40 0.16 2.69 6.59 3.23 0.27 0.07 0.10 95.86TR - 216 55.68 1.33 14.33 10.58 0.18 2.93 7.12 3.27 0.25 0.10 0.13 95.89

Std. Runs (N=73; 2 std. runs per sample analysis)Average 50.76 1.88 13.84 12.12 0.27 6.82 10.83 2.83 0.19 0.23 0.04 99.81Sigma 0.35 0.04 0.13 0.25 0.04 0.07 0.09 0.08 0.01 0.04 0.01 JDF-D2 50.80 1.89 13.8 12.17 0.22 6.83 10.80 2.77 0.22





Shallow intrusive directions of sheeted dikes in the Troodos ophiolite: Anisotropy of magnetic...

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