59. CYPRUS EVAPORITES

Theodoulos M. Pantazis, Geological Survey Department, Nicosia, Cyprus

ABSTRACT

The island of Cyprus is divisible into three major stratigraphicand tectonic zones. The Troodos zone in the south, consists of anigneous massif which occupies the core of the mountain range andhas gently dipping sediments which are peripheral to the massif.

The Pentadaktylos (Kyrenia) zone, in the north, in contrast tothe Troodos massif, is strongly folded and thrusted zone comprisedalmost wholly of sedimentary rocks. The central core of Pentadak-tylos (Kyrenia) range consists of crystallized and semicrystallizedlimestones and dolomites overthrust on younger chalky sedi-ments and turbidites.

The Mesaoria Plain, separating these two zones, is a subsidedarea, which probably continuously received sediments from Cam-panian to late Miocene time. Deep drilling here has shown thatthere are Troodos pillow lavas at the base of this succession, atleast in its southern part.

The Miocene sediments of the Troodos zone are middle Mio-cene marls and chalks with calcarenite layers, fragmented lime-stones, and paper shales (Pakhna Formation). The top of this unitis defined by a prominent stratigraphic marker of up to 5 metersthick of bright white porcellaneous chalks (interbedded with shalylimestone). The porcellaneous chalk has conchoidal fracture andcontains the gigantic foraminifer Discospirina italica (Costa). Thetop of the Pakhna sequence includes bioclastic algal and reeflimestones (Koronia Formation) which grade upwards and later-ally into evaporites consisting mainly of gypsum (KalavasosFormation). Salt has been found only in the northern part of thiszone underlying Pliocene sediments.

The gypsum in the evaporites is of three main varieties: (1) thecommon medium- to coarse-grained saccharoidal type, (2) selenite,forming translucent bladed folia or rosettes, and (3) the marmaratype, a compact medium-grained gypsum which splits into thinflags and is used by villagers for interior flooring tiles.

The middle Miocene sediments in the Mesaoria and Pentadakty-los (Kyrenia) zones are mainly thick (exceeding 3000 m), stronglyfolded deposits of the Kythrea Formation. The Kythrea flyschconsists of thin-bedded arenaceous sediments (turbidites, gray-wackes, etc.) interbedded in places with marl and thin-beddedcalcarenitic limestones. Basal conglomerates are locally present atthe base of this flysch formation.

Overlying the Kythrea turbidites are rather localized outcrops ofpale gray and brown marl of the Pakhna Formation capped insome areas by hard porcellaneous chalks interbedded with paperyshales of the Discospirina Zone. The papery shales are similar tothose of the circum-Troodos Discospirina Zone.

Numerous gypsum outcrops within the arcuate belt of the Mesaoria zoneand the southern periphery of the Pentadaktylos (Kyrenia) range correlateboth lithologically and stratigraphically with the circum-Troodos evapo-rites.

In the northern part of the Pentadaktylos (Kyrenia) zone, theMiocene stratigraphy is similar to that of the southern part of thesame zone, but no gypsum crops out in this area.

Post-Pakhna sediments in all three zones consist of lowerPliocene gray and yellowish brown marls, chalky marls, limestones,and calcarenites (Nicosia Formation) and are overlain by Pleisto-cene sediments.

1185

T. M. PANTAZIS

DISTINCTIVE GEOLOGIC FEATURES OFCYPRUS

The island of Cyprus is dominated by two mountainranges which are separated by an almost east-west-trending plain (Figures 1, 2). These geomorphologicalregions coincide with three major stratigraphic andtectonic zones (Figure 3).

The Troodos zone (Figure 3) consists of an igneousmassif which occupies the core of the mountain rangesurrounded by gently dipping sediments. The igneousmassif is a typical ophiolite consisting of plutonic dykeand pillow lavas. The plutonic rocks occupy the core ofthe massif and are enclosed within a diabase dykeintrusive complex. The pillow lavas, believed to beCampanian in age, form the outer periphery of theophiolitic complex and consist of well-formed pillowsincluding several dykes.

The earliest autochthonous sediments overlying theTroodos massif are comprised of iron- and manganese-rich fine-grained sediments, radiolarites of the sporadi-cally outcropping Perapedhi Formation, and Campa-nian bentonitic clays and volcanogenic sandstoneswhich crop out extensively in the southwestern part ofCyprus (Moni Formation).

The Moni clays are overthrusted by the Mamoniacomplex, an assemblage of broken sheets and isolatedblocks of variable size consisting of sandstones, manga-niferous shales and cherts, lavas intercalated withlimestones, serpentinites, amphibolite schists, reef lime-stones, and pelagic limestone. The age of sediments ofthe Mamonia complex ranges from Triassic to Jurassic,but its emplacement took place during late Campa-nian/early Maestrichtian during which time folding,faulting, and slumping resulted in the formation of anextensive melange.

Overlying the pre-upper Maestrichtian sediments isthe Lefkara Group of Maestrichtian to early Mioceneage. It consists of pelagic marl, bright white chalk withspectacular bedded and nodular cherts, and chert-freebright white massive or cleaved chalks. At the top ofthe sequence the chert-free chalks are interbedded withcoarse-grained bioclastic limestones indicative of ashallow marine depositional environment. In someareas these limestones grade laterally into the reefallimestones of the widespread formation known as theTerra limestones.

Resting on the Lefkara chalks, in most places un-comformably, are cream or light brown middle Mio-cene marls and chalks with distinctive calcarenite,fragmented limestones, and paper shale layers (PakhnaFormation). The top of the Pakhna sequence includesbioclastic algal limestones and reefal limestones (Koro-nia Formation) which grade upward and laterally intoevaporites (mainly gypsum) of the Kalavasos Forma-tion. Salt has only been found in the northern part ofthis zone under Pliocene sediments.

Post-Pakhna sediments consist of lower Pliocenegray and yellowish brown marl, chalky marl, lime-stone, and calcarenite (Nicosia Formation, includingMyrtou marls) overlain by Pleistocene sediments(Athalassa and Kyrenia formations). The terrace de-

posits are conglomerates which fan away from theTroodos massif, and calcarenite or pebble beds whichfringe the coast and form several distinct terraces.

The Pentadaktylos (Kyrenia) zone (Figure 3), incontrast to the Troodos massif, is strongly folded andthrusted and is composed almost entirely of sedimen-tary rocks. The central core of Pentadaktylos consistsof crystallized and semicrystallized limestones anddolomites which have been thrust over onto youngerchalky sediments and turbidites.

The crystallized and semicrystallized limestones anddolomites of the core of Pentadaktylos (Kyrenia) zoneare collectively called the Hilarion Limestones. Thesehave recently been found to comprise a number ofdistinct formations of Triassic, Jurassic, and Early orprobably Middle Cretaceous age (Dhikomo, Sykhari,and St. Hilarion formations), together with blocks ofPermian limestones.

The Hilarion rocks are thrusted over fine-grainedlimestones which extend laterally into chalks, marlylimestones, and clays, (Lapithos Formation). Sandylimestones and flows or sills of pillow lavas andgabbroic rocks form the base of this Campanian orMaestrichtian succession. The Hilarion rocks also haveclays and olistholiths which correlate to the MoniFormation. Upper Eocene-Oligocene coarse-grainedlimestones occur laterally and at the top of the succes-sion (Ardana-Kalogrea Formation).

Intensely folded turbidite (flysch) deposits fringe thePentadaktylos (Kyrenia) range. Their deposition beganin the late Eocene or Oligocene and continued intomiddle Miocene time, but most turbidites were depos-ited in middle Miocene (Vindobonian). The youngerturbidites are called the Kythrea Formation.

The upper part of the Kythrea Formation gradeslaterally and upward into calcareous sediments andevaporites (gypsum deposits) which correlate to thecircum-Troodos, Pakhna, Koronia, and Kalavasos for-mations. Also, the Pliocene and Pleistocene deposits ofthis zone are similar to the circum-Troodos Pliocene-Pleistocene sediments.

The Mesaoria plain (Figure 1) is a subsided areawhich probably received sediments continuously duringthe Campanian to late Miocene time. Deep drilling hasshown that Troodos pillow lavas are present at thebase of this succession, at least in its southern part. Thelower Pliocene and Pleistocene deposits extend to boththe northern and southern zones. At the eastern andwestern parts of the Mesaoria plain two recentlyformed basins are filled with Recent sands, gravels,and silts. In general, the southern part of Mesaoria issimilar to the Troodos zone and the northern part issimilar to the Pentadaktylos zone.

MIOCENE-PLIOCENE STRATIGRAPHY ANDEVAPORITE FACIES

Deposits Surrounding the Troodos Massif (Figures1, 2, 3)

The gypsum deposits surrounding the Troodos mas-sif are most extensively developed in the southern partwhere the Pakhna Formation is best developed. In this

1186

32°3σ

CONTOUR MAP OF CYPRUS

FACIES MAP OF THE LATE MIOCENE IN CYPRUSCompiled by Th.M.Pantazis, Ph.D.,D.I.C.,F.I.M.M

1976

L E G E N DPliocene, Pleistocene and Recent Deposits

Reef Limestone Koronia Formation

Offshore evaporites with mainly sulfatic facies

Offshore evaporites with thick salt layers

Kalavasos Formation

Pakhna Formation

j : : : : : | Salt (une×posed)

Outcropping Gypsum

fc >X x] Subsurface Gypsum

Discospirina bandChalks, Marls and Limestones

Turbidites and Marls, Kythrea Formation

Reef Limestone,Lefkara Group (Upper)

Pre-Neogene Formations ( Tectonised or not)

Troodos Ophiolitic Massif

— * — OverthrustsI, Boreholes

—400— Bathymetry in metresA—A' Section lines

Figure 1. Facies map of the late Miocene in Cyprus.FIG. 1 Drawn by Geological Survey Department, Cyprus,

T. M. PANTAZIS

12(EB22)

22

Sea level _ATroodos (P408) Mesaoria Pentadaktylos__ i ; River ;

Sea level

TroodosRiver

Mesaoria Pentadaktylos

J*_ Sea level

Projection of

(PB49) (PB47)

C-C SCALE1I

2 kms

Figure 2. Diagrammatic geological sections along A-A', B-B', and C-C'.

region (Figures 1, 2) the Pakhna Formation consists ofa thick (up to 600 m) succession of marls, chalks, andlimestones. It forms three distinct lithological facies,each of which extend over a large geographical area.

The lowest part of the Pakhna succession is com-posed of a rhythmic sequence of yellow to buff marlsand marly chalks or limestones which unconformablyoverlie the Lefkara chalks (Gass, 1960; Bagnall, 1959;Bear and Morel, 1960; Pantazis, 1967). The uncon-formity, however, is not present in areas where deposi-tion of the Lefkara Group sediments continued into theearly Miocene (Pantazis, 1967). Further to the west,and particularly in the Polis basin, the Pakhna sedi-ments may also unconformably overlie lower Miocenereef limestones of the Lefkara Group. The basalsediments of the Pakhna Formation are generally fine-to medium-grained with a few coarse-grained shellybeds (bioclastic limestones) containing grains of ferro-magnesium silicates identical to those of the Troodosophiolitic rocks. The percentage of marl in relation tothe chalks or limestones varies both laterally andvertically, but the thicker deposits of marls are usuallyfound near the top of the sequence. At the contactbetween the Troodos tectonic zone and the Mesaoriaplain the marls of the Pakhna Formation consist ofnormal Pakhna sediments mixed with turbidite mate-rial. The top of this unit is marked by a prominent5-meter-thick bed of bright white porcellaneous sili-ceous chalk interbedded with shaly limestone. The

porcellaneous chalk has a characteristic conchoidalfracture and includes the gigantic foraminifer, Disco-spirina italica (Costa). This zone known as a Discospir-ina band is very extensive, traceable for many kilome-ters, but it may not necessarily be present at everyPakhna exposure.

The chalk-marl sequence grades both vertically andlaterally, but most typically vertically into a calcareniticor fragmental shaly limestone facies.

The calcarenites are massive, coarse-grained, yel-lowish brown, bioclastic limestones with interbeddedclastic Troodos igneous material and shaly limestone.

The fragmented shaly limestone crop out over aconsiderable area, but is probably the thinnest unit ofthe Pakhna Formation. These thin bedded limestonesresemble paper shales and are interbedded with flaggylimestones and marls. The fragmented shaly limestonesare medium- to fine-grained with very distinct currentbedding structures. They are fossiliferous and in someplaces contain large fossilized fish. Hard, compact,bioclastic bioherm and biostrom limestones of theKoronia formation, which mark the end of the calcare-ous sedimentary cycle of middle Miocene, conformablyoverlie the Pakhna Formation. The formation is alsotransgressive and, in places, overlies older formationsincluding igneous rocks. This reef limestone gradesupward and laterally into evaporites (gypsum) of theKalavasos Formation and forms extensive outcrops. Allworkers agree that the Koronia Formation grades

1188

CYPRUS EVAPORITES

PERIODS GROUP! FORMATIONS

TROODOS MESAORIA PENTADAKTYLOS (KYRENIAGROUPJ FORMATIONS

UPPER

ATHALASSA

NICOSIA

TERRA LIMESTONE

MAESTRICHTIAN

PAREKKLISHA ANDAKAMAS

TROODOS OPHIOLITICCOMPLEX

Silts, Sands and Gravels

Conglomerates andCalcarenites

Calcarenites andMarly Limestones

Calcarenites,Marly Limestones andMarls

Gypsum and Salt

Reef Limestone

Discospirina Band

Calcarenites, Limestones,Marly Chalks, Marls andBioclastic Limestones

Reef Limestone

Bright white Chalks

Bright white Chalksinterbedded with Cherts

Sandstones and QuartzitesIron and Manganese-richsiltstones and mudstonesPillow Lavas

Plutonic Rocks

JURASSIC

Clays

PENDAKOMO

PETRA TOUROMIOU

Radiolarian Limestone

Thin-bedded Radiolantes

Reef Limestone

Daonella Limestone,Ammonite Limestone andSandstones

mSilts, Sands and Gravels

Conglomerates.Calcarenites andTravertinesCalcarenites andMarly Limestones

Calcarenites,Marly Limestones andMarls

Gypsum

Limestones and Marls

Turbidites (flysch)

Basal Conglomerate

Turbidites interbedded withBreccias

NICOSIA

KALAVASOS

PAKHNA

KYTHREA

BELLAPAISOR

ARDANA-KALOGREA

Globigerinal Limestonewith ChertsCalcarenites

Globigerinal Limestone

Pillow Lavas and RhyolitesGabbroic SillsSandy LimestoneBrecciasMelange 1 Clays with

| Olistholiths

Marbles and

Recrystallized Limestones

Dolomitic Limestone

Recrystallized and BrecciatedDolomitic Limestone

LAPITHOS

ISu 5

Marbles with Phyllites

% I , Limestones in places

/ T T T T Recrystallized

ST. HILARION

SYKHARI

DHIKOMO

Only as Olistholithsin Lapithos Formation

Note : The stratigraphic columns are not drawn in scale and do not correspond to the thickness of the lithological units.

Figure 3. Stratigraphy of the tectonic zones of Cyprus.

upward into gypsum deposits, and some (Cleintuar etal., in press) regard the lateral variation of reefs intogypsum as probable. Note, however, that in the southcentral area, loronia reef limestones were found tointerbed with gypsum bands (Pantazis, 1967) andrecent drilling in the most western part of the area(Polis basin) showed that gypsum is a lateral faciesvariation of Koronia reef limestones (Figures 2 and 4).

Four main types of gypsum occur in Cyprus: (1)saccharoidal, (2) selenite, (3) "marmara," and (4)alabaster. The results of chemical analyses of repre-sentative samples from all these types of gypsum,including one alabaster type, are given in Table 1.

1) The saccharoidal gypsum is medium- to coarse-grained, dull brownish gray or white, and massivelybedded. In thin section it is seen to consist of mutuallyinterfering broad plates and subhedral aggregates ofgypsum which usually show a perthitic-like texture andpolysynthetic twinning. Some recrystallized platy gyp-sum also occurs along the bedding or the joint planes.The saccharoidal variety is the most common gypsumin Cyprus and is the main type quarried for export.

2) The selenite gypsum is found closely associatedwith the saccharoidal variety. It is colorless and trans-lucent and forms bladed folia, aggregates, or "ro-settes." The bladed folia are composed of large, (up toabout two feet long) glistening, laminated, platy sele-

nite crystals which are flattened parallel to the (010)crystallographic faces. The foliation is very well de-fined and is a result of prominent cleavage parallel tothe (010) crystallographic faces. The aggregates consistof thin unoriented radiating folia of selenite. The"rosettes" are composed of similar thin folia of trans-lucent selenite but radiate from a central point.

3) The marmara is a compact, generally of gray-ish or brownish white medium-grained gypsum, whichusually splits into flags one to two inch thick. Thisvariety is found in the surveyed area interbedded withthe saccharoidal gypsum and may include anhydrite. Itis used by the villagers for interior floor tiles andcourtyard paving slabs. In thin section the marmarashows textures similar to the saccharoidal type.

The outcrops of the Nicosia Formation are restrictedto the southwest part of Cyprus and usually consist ofbuff colored, fossiliferous, calcarenite and marls. Theyunconformably overlie the Pakhna Formation or thegypsum deposits. Recent drilling in the area (Figure 3)has shown, however, that all unexposed gypsum depos-its underlie lower Pliocene marls.

In many places the Pliocene sediments underliePleistocene deposits consisting of calcarenites, sands,gravels, and conglomerates. They form several distinctterrace deposits which fringe the coastline of southernand southwestern Cyprus.

1189

T. M. PANTAZIS

Metres200

(DPB49

(2)

PB50

(5)

PB60

(6)

PB59

...o.Saa.!ftval.

-50

—100

—150

-200

—250

—300

—350

π S Gdi

Gne

(3)

PB47

(4)

PB48

Gps

Gme

Gne

IvGps

Sdei

Gma;

Gps

Gme

Gdi

Metres

200

1 5 0 -

100

50

eyβ!..o

- 5 0 -

FORAMINIFERAL ZONING By M. MANTIS

Zones Abbreviation

Globorotalia crassaformis

Sphaeroidinella dehiscens

Globorotalia margaritae

Globorotalia pseudomiocenica

Globorotalia menardii

Globigerina nepenthes

Globigerinita dissimilis

Pre-Neogene

Gcr

Sdh

Gma

Gps

Gme

Gne

Gdi

[ Z

Figure 4. Detailed borehole records ofPolis basin area. Foraminiferal zoning by M. Mantis.

TABLE 1Chemical Analyses of Gypsum

Analysis

Free waterCombined waterCarbon dioxide (CO2)Silicon dioxide (Siθ2) and

insoluble matterIron and aluminum (Fe2θj + AI2O3)Lime (CaO)Magnesium oxide (MgO)Sulfur trioxide (SO3)Sodium chloride (Nacl)Total

Report of ResultsGypsum (CaSO4.2H2O)Anhydrite (CaSO4)Silicon dioxide + insolublesIron and aluminum (R2O3)Calcium carbonate (CaCOj)Magnesium carbonate (MgC03>Sodium chloride (NaCl)Total

Marmara

2 samplesmean value (%)

0.0419.72

1.581.04

0.3832.32nil

44.89—

99.97

94.221.821.040.381.88

nil-

99.34

Saccharoidal

2 samplesmean value (%)

0.0320.35

0.250.88

0.3031.70nil

46.45-

99.96

97.231.150.880.300.20

nil-

99.76

Exported type17 Samples

mean value (%)

0.0119.41

0.971.07

0.2032.67

0.0545.17

0.0199.56

92.743.481.070.201.850.100.01

99.45

Selenite

2 samplesmean value (%)

0.0520.43

0.120.70

0.2431.75nil46.95

-100.24

97.601.550.700.24

nilnil

-100.09

Alabaster

1 sample (%)

0.0320.58

0.060.70

0.2031.85

nil47.15

—100.57

98.331.150.700.20nilnil

-

100.38

In contrast to the southern region, the PakhnaFormation forms restricted exposures of sediment andgypsum in the northern part of the Troodos rangewhich led earlier authors (Gass and Cockbain, 1962)to believe that occurrence of these formations wasextremely localized. As a result of recent drilling,however, thick deposits of both Pakhna sediment andgypsum have been found. The stratigraphic relation-ship between the Pakhna sediment and gypsum depos-its and associated sediments, as shown from the out-crops and the boreholes, is similar to that of thesouthern region surrounding the Troodos range. ThePakhna sediments show distinct current bedding andthe gypsum deposits generally thicken toward the westfrom about 30 meters in the central north region toabout 200 meters at the most northwestern part (Mor-phou Basin). The gypsum, relative to the Pakhna

sediments, also thickens toward the east and is about100 meters thick at Famagusta. This gypsum includesan increased number of clay bands.

All buried gypsum deposits (Figure 3) were foundunderlying lower Pliocene marls, which form extensiveoutcrops in this area, and overlying Pakhna marls orreef Koronia limestone. It is clear that the hard porcel-laneous chalks interbedded with papery shales (Disco-spirina band) mark the top of the Pakhna marl-chalksequence and underlie the gypsum deposits (Gass andCockbain, 1962). In the southern region there aremarly bands at the base of the gypsum but because oflimited exposure of Pakhna sediments in the northernregion, a complete facies study is not possible.

South of Nicosia at Xeri (Figure 2) a borehole (No.22, P408) penetrated a body of rock salt between 884meters and 1189 meters. Of this, 296 meters consists of

1190

T. M. PANTAZIS CYPRUS EVAPORITES

pure salts, the remaining 9 meters is gray marl contain-ing anhydrite (Gass, 1960). The rock salt thus com-prises two distinct bands. This deposit underlies lowerPliocene marls which contained shell fragments and abasal unit composed of gray marl with fragments ofchalk, igneous rocks, and gypsum. The salt overliesgray marls with anhydrite and shale fragments.

Mesaoria and Pentadaktylos (Kyrenia) Zones

The middle Miocene sediments in the Mesaoria andPentadaktylos (Kyrenia) zones are mainly thick depos-its (exceeding 3000 m) of the strongly folded KythreaFormation (Figures 1, 2). The Kythrea flysch consistsof thin-bedded arenaceous sediments (turbidites, gray-wackes, etc.) interbedded, in places, with marls andthinly bedded calcarenitic limestones. Basal conglomer-ates at the base of this flysch occur in some places.

Pale gray and brown marls of the Pakhna Forma-tion overlie the Kythrea turbidites. The Pakhna For-mation is capped in some areas by hard porcellaneouschalks interbedded with papery shales of the Discospir-ina Zone which is similar to the circum-TroodosDiscospirina band. The Pakhna sediments have rela-tively low dips compared to the dips of the underlyingKythrea beds. There probably is an angular uncon-formity between the two units. Gypsum in the Mesao-ria zone and the southern Pentadaktylos peripheryconformably overlies the Pakhna sediments. It is up to25 meters thick and includes marly material in someplaces.

Numerous gypsum deposits which extend from themost western part to the most eastern part of Cypruswithin the arcuate belt of the Mesaoria zone and thesouthern periphery of the Pentadaktylos range wereincluded by Henson et al. (1949) under the heading ofthe "Lapatza gypsum lentil." In this zone the gypsumoccurs at the top of a succession of calcareous sedi-ments. In some cases the beds underlying the gypsumare not exposed, and at other localities, althoughsediments typical of the succession are present, theuppermost gypsum has either been removed by latererosion or was not deposited. A generalized successionby Gass and Cockbain (1962) is as follows:

Thickness (m)

Gypsum with gray gysiferous marls 0-25Hard porcellanous chalks {Discospirina

band) with papery shalesPale gray and brown marls

5-916-55

The gray and brown marls at the base of thesuccession are particularly well exposed at the typelocality and in a few other places. They are soft, poorlybedded, and are of the same color as the sediments ofthe underlying Kythrea Formation. There is considera-ble variation in the thickness of marls present. Thealternating gray and brown banding is typical of thispart of the sequence. The hard porcellaneous chalksoccur in a narrow zone and stand out prominentlyagainst the smooth slopes formed by the underlyingmarls. They include three or four bands of hard whitechalk separated by pale-gray and buff papery shales

with Discospirina italica in the uppermost chalk bands.The gypsiferous horizons occur immediately abovethese beds. At the surface the gypsum is usually in theform of coarsely crystalline selenite which usuallyoverlies the bedded variety of gypsum known locally asmarmara. Complex minor plications are commonlypresent in the bedded gypsum. Detailed mapping ofthe junction between the Lapatza gypsum outcrops andthe underlying turbidites of the Kythrea Formation(Moore, 1960) suggests that this contact is an uncon-formity. Although no exposure of this junction has yetbeen found, outcrops within a few feet of the contactindicate that it is probably an angular unconformity.The strike of both formations is conformable but thereis a marked discrepancy in the angle of dip betweenbeds of the Lapatza outcrops and those of the underly-ing Kythrea Formation. The dip of the Kythrea For-mation is usually greater than 30°, whereas the dip ofthe Lapatza sediments, except in a few contorted areas,is well below this figure.

Micropaleontological (Gass and Cockbain, 1962)and stratigraphic evidence indicates that the "LapatzaGypsum Lentil" can be correlated with the circum-Troodos gypsum (Kalavasos Formation).

PALEONTOLOGY

The foraminiferal faunas from the upper PakhnaFormation and the Lapatza gypsum outcrops havebeen examined by Gass and Cockbain (1962) in orderto determine the age and correlate the two formations.Particular attention was paid to the Pakhna Formationwhich is on the north side of the Troodos massif, andwhere the stratigraphical succession is very similar tothat of the Lapatza gypsum. Two faunal assemblageswere recognized by Gass and Cockbain in the chalksand marls of both formations as follows. The lowerbeds contain numerous anomalinids and globigerinids,along with lagenids; in the upper part of the sequencea few buliminids are found. The anomalinid-globig-erinid assemblage occurs throughout the lower portionof both the upper Pakhna Formation on the northernflank of Troodos, and in the Lapatza gypsum outcrops.About 3 to 5 meters below the level of the Discospirinaband it is replaced by the buliminid assemblage. Thefauna is characterized by an abundance of planktonicforaminifers and such benthic species as Anomalinahelicina and Cibicides pseudoungerianus. In addition,several species of Robulus occur in the Pakhna out-crops.

The buliminid assemblage occurs in the upper 3 to 5meters of both the Pakhna Formation and the Lapatzagypsum chalks. The upper limit is approximately at thehorizon of the Discospirina band. Discospirina itself isusually confined to the hard chalk band to which itgives its name.

The buliminid assemblage occurs over a wide areaand, because of its limited vertical range it providesstrong evidence in favor of correlation of the upperPakhna with the Lapatza gypsum outcrops. Completefaunal lists are found in Gass and Cockbain (1962)and Henson et al. (1949). Both papers recorded essen-tially the same fauna from the Lapatza gypsum lentil.

1191

A recent stratigraphic and micropaleontologic workon the Neogene sediments of the Pentadaktylos (Kyre-nia) and Mesaoria zones by Baroz and Bizon (1974)revealed nine formations ranging in age probably fromlate Eocene to the evaporitic Messinian and showedthat the Pliocene sediments were transgressive andrepresent a new sedimentation cycle.

Several planktonic foraminiferal biozones have beenidentified. Their succession is quite similar to thatfound from the Oligocene to the middle Pliocene in thewestern Mediterranean.

The Kythrea Formation belongs to two physio-graphic provinces separated by the large east-west-trending Kythrea fault. In the northern "Pentadak-tylian" province, a relatively diversified transgressiveseries was deposited. In the southern "Mesaorian"province, the sedimentary series lies conformably onchalky deposits which extends southward towardsTroodos.

A zonation proposed for the Pentadaktylos and thenorthern Mesaoria by Bizon (in Baroz and Bizon,1974) is shown in Figure 5. Figure 6 shows theforaminiferal zoning of Cyprus as proposed by Mantis.

MIOCENE-PLIOCENE TECTONIC HISTORY OFCYPRUS

The three tectonic zones of Cyprus namely theTroodos, Pentadaktylos (Kyrenia), and Mesaoria havedistinct tectonic characteristics.

In the Troodos zone there is strong evidence tosuggest that the central part of the massif was abovesea level at the end of Lefkara Group deposition andremained above sea level since lower Miocene. The sealevel however was not stable as a deepening of themiddle Miocene basin occurred with the beginning ofPakhna sedimentation which then decreased until atime when the water depth was shallow enough toallow the deposition of reef and algal limestones(Koronia Formation) and evaporite deposits (Kalav-asos Formation). The formation of reefs or the deposi-tion of evaporites were controlled by the local condi-tions which existed at the time around the TroodosIsland. The middle Miocene reefs are transgressiveoverlying, in places, the Troodos volcanic rocks. Thegypsum, however has not been found overlying suchrocks. The middle Miocene sedimentation was fol-lowed by a period of more uplift and erosion of themassif. The next cycle of sedimentation took place inthe lower Pliocene after the massif sunk to such adepth that Pakhna sediments and perhaps the outerzone of Lefkara Group rocks were submerged. Thelithologies of the lower Pliocene sequence are mainlymarls, at the deepest parts, with calcarenite or marlylimestone elsewhere.

In the Pentadaktylos zone, forces directed from thenorth during the Attican phase in late Miocene causedlow-angle folding and thrusting of large and elongatedslices of Paleozoic rocks, recrystallized lower Mesozoiclimestone, and other pre-Miocene rocks (Henson et al.,1949; Moore, 1960). By the end of Miocene thePentadaktylos (Kyrenia) range emerged from the sea

and formed an elongated, arcuate, low-level range.The Pliocene and Pleistocene geological history of thiszone is similar to that of the Troodos range.

The Mesaoria zone has been a deep basin betweenthe two other zones probably since Eocene times. Themovements which occurred towards the end of Mio-cene caused intense folding of the sediments intonarrow synclines and anticlines. As a result of thefolding the Mesaoria base was raised to near the sealevel, but its central part (a zone running from east towest) probably remained below sea level continuouslyuntil the end of the Pliocene while the other two zonesemerged from the sea.

The general uplift of the Troodos and Pentadaktylos(Kyrenia) range at the end of Calabrian was followedby uplift of the Mesaoria plain which brought it abovesea level and joined the two islands into one. Furthergeneral uplift occurred in all three zones and resultedin the formation of a number of marine terracesfringing the coast lines and river terraces lining therivers of Cyprus.

Alpine orogenic movements did persist into Pleisto-cene time, but resulted only in faulting and some tiltingof the younger sediments.

ACKNOWLEDGMENTS

I express sincere thanks to Dr. L. Montadert for providingthe guidelines for this paper and for his invitation to Francewhere discussions with him and his staff, Dr. B. Biju-Duvaland Mrs. G. Bizon, were very helpful. He also criticallyreviewed the manuscript. I thank also my colleagues, S.Afrodisis, S. Zomenis, M. Mantis, and Chr. Constantinou forproviding drilling and other useful data, and Prof. G.Paraskevopoulos and Prof. Gr. Marakis for their helpfuldiscussions.

REFERENCES

Bagnall, P. S., 1959. The geology and mineral resources ofthe Pano Lefkara-Larnaca Area: Mem. Geol. Surv. Dept.Cyprus No. 5, p. 1-116.

Baroz, F. and Bizon, G., 1974. Le Neogene de la chaine duPentadactylos et de la partie nord de la Mesaoria (Chy-pre). Etude stratigraphique et micropaleontologique: Rev.Inst. France Petrol, v. 29, p. 327-359.

Cleintuar, M. R., Knox, G. J., and Ealey, P. J., in press. Thegeology of Cyprus and its place in the East-Mediterraneanframework.

Gass, I. G., 1960. The geology and mineral resources of theDhali Area: Mem. Geol. Surv. Dept. Cyprus, No. 4, p.1-116.

Gass, I. G. and Cockbain, A. E., 1962. Notes on theoccurrence of gypsum in Cyprus. Overseas: Geol. andMin. Res., v. 8, p. 279-287.

Henson, F. R., Browne, R. V., and McGinty, J. 1949. Asynopsis of the stratigraphy and geological history ofCyprus: Quart. J. Geol. Soc. London, v. 105, p. 1-41.

Moore, T. A., 1960. The geology and mineral resources ofthe Astromeritis-Kormakiti Area: Mem. Geol. Surv. Dept.Cyprus, No. 6, p. 1-96.

Pantazis, T. M., 1967. The geology and mineral resources ofthe Pharmakas-Kalavasos Area: Mem. Geol. Surv. Dept.Cyprus, No. 8, p. 1-190.

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