ORIGINAL ARTICLE

Topography controlling the wind regime on the karstic coast:late Pleistocene coastal calcareous sands of easternmid-Adriatic, Croatia

Davor Pavelic • Marijan Kovacic • Igor Vlahovic •

Oleg Mandic • Frane Markovic • Lara Wacha

Received: 25 March 2014 / Accepted: 25 July 2014 / Published online: 26 August 2014

� Springer-Verlag Berlin Heidelberg 2014

Abstract Aeolian dunes controlled by regional climate

have been formed in many coastal areas of the Mediter-

ranean Sea during the Quaternary. Generally, they are

formed under a landward-blowing wind, and comprise

numerous reworked penecontemporaneous shallow-marine

carbonate grains. Along the eastern mid-Adriatic Sea, late

Pleistocene aeolian and alluvial sands occur as isolated

patches in karstic depressions on several islands and the

Peljesac Peninsula. At most localities, the sands consist of

a mixture of mostly carbonate rock fragments and silici-

clastic material. A higher proportion of shallow-marine

bioclasts was found only at one locality. The terrestrial

material was transported to the coastal area by at least two

rivers: paleo-Cetina and paleo-Neretva River, and was

subsequently reworked and transported by wind, resulting

in aeolian deposition. Sandy units of various thicknesses

exhibiting sharp erosional bedding planes and cross-bed-

ding are interpreted as representing aeolian dunes and sand

sheets controlled by a complex wind regime. The miner-

alogical composition at almost all localities indicates near-

river flood plains as the main sand source. Although the

area was affected by strong winds blowing landward and

parallel to the coast, they significantly deviated due to the

local topography produced by the tectonically deformed

and karstified carbonate basement. In this way, the late

Pleistocene aeolian deposits on the mid-Adriatic islands

differ from deposits from most Quaternary Mediterranean

coastal aeolian belts, as they contain very small quantities

of penecontemporaneous shallow-marine carbonate grains

and were deposited by winds blowing in varying directions

instead of prevailing landward-blowing winds.

Keywords Inland aeolian dunes � Alluvial deposits �Provenance � Wind regime � Late Pleistocene �Mid-Adriatic islands

Introduction

Aeolian dunes in coastal areas share some common char-

acteristics, even if formed in different climatic belts char-

acterized by specific regional wind regimes. Along many

coasts of the world, dunes are formed by landward-blowing

winds, causing onshore movement of sand (Pye and Tsoar

2009). This is also a characteristic feature of Mediterranean

coasts, where seaward sand migration is uncommon and

has been found at just a few localities, such as the Libyan

coast where bimodal paleowind directions prevailed in the

Pleistocene (Hoque 1975), and the Croatian mid-Adriatic

islands (Pavelic et al. 2011; Babic et al. 2012, 2013). The

modern Tunisian coast is also characterized by strong

seasonal changes in wind directions. Landward-blowing

winds control dune migration during the summer, whereas

the winter is characterized by seaward blowing winds

causing truncation of the dunes formed in the summer

(Hasler et al. 2012). Coastal aeolian sands may contain a

D. Pavelic (&) � I. Vlahovic

Faculty of Mining, Geology and Petroleum Engineering,

University of Zagreb, Pierottijeva 6, 10000 Zagreb, Croatia

e-mail: dpavelic@rgn.hr

M. Kovacic � F. Markovic

Faculty of Science, University of Zagreb, Horvatovac 95,

10000 Zagreb, Croatia

O. Mandic

Geological–Paleontological Department, Natural History

Museum Vienna, Burgring 7, 1010 Wien, Austria

L. Wacha

Croatian Geological Survey, Sachsova 2, 10000 Zagreb, Croatia

123

Facies (2014) 60:843–863

DOI 10.1007/s10347-014-0411-7

substantial proportion of shallow-marine carbonate grains,

such as bioclasts, foraminifers, peloidal grains, and ooids

(McKee and Ward 1983). These carbonate grains typically

originate from subaerially exposed marine beach sands that

are picked up by wind together with detrital grains and

subsequently were deposited on the backshore creating

calcareous dunes (McKee and Ward 1983; Brooke 2001;

Le Guern and Davaud 2005; Frebourg et al. 2008; Mauz

et al. 2013).

Late Pleistocene aeolian sands occur at several places

along the northeastern coast of the Adriatic Sea and are

exposed on the mid-Adriatic islands of Hvar, Vis, Mljet,

Lastovo, and Korcula (Fig. 1). The aeolian sands are

intercalated with alluvial sands and breccias, which may

Fig. 1 Location map showing position of Croatia (in grey) within SE

Europe and localities studied. The Dinarides are subdivided into the

Karst Dinarides (or External, or Outer Dinarides) along the Adriatic

Sea, and the Inner Dinarides (or Internal Dinarides) between the Karst

Dinarides and the Pannonian Basin as shown in the upper right figure.

Numbers in the lower figure represent present-day heights above sea

level and water depths around the mid-Adriatic islands and the

Peljesac Peninsula. The locations studied are marked by black dots

and bold lettering. Rose diagrams represent relative frequency of

individual wind directions measured at the weather stations from

1981–2012 (data provided by Croatian Meteorological and Hydro-

logical Service, Zagreb). Partly modified after Pavelic et al. (2011)

844 Facies (2014) 60:843–863

123

also form individual accumulations (Markovic-Marjanovic

1976, 1979; Borovic et al. 1977; Korolija et al. 1977;

Bognar et al. 1992; Pavelic et al. 2011; Babic et al. 2012,

2013). Intercalation of aeolian and fluvial/alluvial deposits

is a common facies association, and has been described

from many modern and ancient inland and coastal envi-

ronments worldwide (e.g., Brookfield 1979; Clemmensen

and Abrahamsen 1983; Langford 1989; Langford and Chan

1989; Clemmensen et al. 1994; Rose et al. 1999; Mountney

and Thompson 2002; Andreucci et al. 2006; Rodrıguez-

Lopez et al. 2011; Luzon et al. 2012; Gil et al. 2013).

The aeolian deposits on the mid-Adriatic islands have

been recently studied in more detail, and aeolian bedforms,

wind regime, sand source, and climate controls have been

interpreted (Pavelic et al. 2011; Babic et al. 2012, 2013).

However, some interpretations differ, especially regarding

the sand source, which is according to Pavelic et al. (2011)

mostly of fluvial provenance, while Babic et al. (2013)

interpreted them as being of marine provenance. Here we

provide new data on paleowind direction, grain mineral-

ogy, and depositional mechanisms which together improve

the knowledge on probable source areas and wind regime

that operated on the Adriatic coast. The composition of

isolated alluvial sandy deposits as a consequence of recy-

cling of aeolian sand at some of the studied sites (Hvar and

Peljesac) offers additional support for the interpretation of

the provenance area and paleoclimate in the study area

during the late Pleistocene.

The aim of this study is to highlight the presence of

coastal belts of aeolian sands transported by landward- and

seaward-blowing winds, which moreover deviated due to

the local topography produced by the tectonically

deformed karstified carbonate basement. This differs from

most of the Mediterranean coasts, where the dominant

winds blew landward at most places, like the coasts of

Mallorca (Clemmensen et al. 1997; Nielsen et al. 2004),

Sardinia (Andreucci et al. 2006, 2009), Tunisia (Elmejdoub

et al. 2011; Hasler et al. 2012), Egypt (Frihy et al. 1988; El

Banna 2004) and Israel (Yaalon and Laronne 1971).

Geological setting, geomorphology, and the modern

wind regime

The Adriatic Sea is located in the north-central Mediter-

ranean between the NE coast of Italy and the coasts of

Slovenia, Croatia, Montenegro, and Albania. It is approx-

imately 770 km long, with an average width of about

160 km (Figs. 1, 2). The sea is closed to the north and

connected to the south with the Ionian Sea through the less

than 75-km-wide Strait of Otranto. The northern Adriatic is

relatively shallow with a maximum depth of about 100 m,

while a maximum depth of ca. 1,300 m is reached in the

southern Adriatic.

The study area is located on the NE Adriatic coast in

central and southern Dalmatia (Croatia), and its nearby

hinterland is characterized by a complex geology (Figs. 1,

3). The Dinarides are generally divided into the Karst Di-

narides (or External, or Outer Dinarides) along the Adriatic

Sea, and the Inner Dinarides (or Internal Dinarides) to the

NE. The Karst Dinarides are composed of several thousand

meters of mostly shallow-marine Mesozoic carbonates (see

Vlahovic et al. 2005, and references therein), with subor-

dinate Paleozoic (Sremac 2012) and Cenozoic carbonate

and siliciclastic deposits (Fig. 3). The Inner Dinarides are

composed of variable rock types, ranging from siliciclastic

and carbonate rocks, ophiolites associated with radiolarites,

greywackes and shales, to blueschists, tectonized ophio-

lites, metamorphic rocks, and granitoids (see Pamic et al.

1998, and references therein).

The part of the Karst Dinarides studied mainly belongs

to a group of mid-Adriatic islands of central (Hvar and Vis

Islands) and southern Dalmatia (islands of Korcula, Las-

tovo, and Mljet, and the Peljesac Peninsula) mostly com-

posed of shallow-marine carbonates deposited on the

Mesozoic Adriatic Carbonate Platform. Middle Triassic

rocks as evaporites, magmatic, and siliciclastic rocks occur

only in the westernmost part of Vis Island while Eocene

limestones and siliciclastic deposits occur on Hvar Island

and Peljesac Peninsula (Vlahovic et al. 2005, and refer-

ences therein) (Fig. 3). The study area is characterized by

relatively high relief (highest peaks range from 417 m at

Lastovo to 628 m at Hvar, and 961 m at Peljesac). Mor-

phology of islands commonly corresponds to the geological

structures, with hills representing cores of anticlines com-

posed of Mesozoic carbonates, while synclines composed

of Paleogene clastic deposits usually form valleys.

Late Pleistocene deposits were studied on five mid-

Adriatic islands and the Peljesac Peninsula, with a distance

between the outermost localities, Vis and Mljet, of

approximately 130 km (Figs. 1, 2). The position of the

base of the studied deposits varies between 10 and 115 m

a.s.l. The deposits cover small shallow depressions and

topographic saddles that are the result of tectonic defor-

mation, karstification, and fluvial erosion (Babic et al.

2013). On most of the localities studied, sands crop out at

elevations up to 40 m above the present-day sea level

(a.s.l.), but at Hvar they can be observed up to 85 m a.s.l.

(Pavelic et al. 2011), at Vis approximately to 120 m, and at

Mljet there are occurrences up to 200 m a.s.l. (Markovic-

Marjanovic 1979), indicating a very strong wind that

caused aeolian deposition at such high altitudes (Pavelic

et al. 2011; Babic et al. 2013). The sands on some of the

localities have been determined as late Pleistocene (Wur-

mian), based mainly on mammal associations (Malez 1972;

Markovic-Marjanovic 1976, 1979; Bognar et al. 1992;

Babic et al. 2012, 2013), but absolute dating has not been

Facies (2014) 60:843–863 845

123

provided so far. In the Northern Adriatic, loess intercalated

with aeolian sand has been dated by infrared stimulated

luminescence and radiocarbon dating, showing good cor-

relation with Marine Isotope Stage (MIS) 3 (Wacha et al.

2011a).

At the present day, the entire study area is surrounded

by a relatively shallow sea, with depths mostly between

50 and 120 m (Figs. 1, 2). During late Pleistocene low-

stands, the major part or the area thus represented part of

the mainland characterized by hills of steep relief

separated by large river floodplains (Correggiari et al.

1996; Pavelic et al. 2011; Babic et al. 2013). High alti-

tudes at which studied sands occur could not be reached

by rivers, additionally favoring the aeolian interpretation.

The Last Glacial Maximum lowstand is indicated by

speleothem precipitation in submerged caves at the

Eastern Adriatic coast between 37,000 to 22,000 BP,

which were flooded later by the Late Pleistocene–Holo-

cene sea-level rise (Suric et al. 2005) (Fig. 1); only the

area SW of the Vis–Lastovo line was continuously

Fig. 2 a Bathymetric map of the Adriatic Sea (simplified, after

Hydrographic Institute of the Republic of Croatia, 1994) showing

modern coastline, as well as areas exposed during minor late

Pleistocene glacial sea-level falls (up to 50 m below present sea-

level) and during major sea-level falls (up to 120 m below present

sea-level). b Inset showing detailed bathymetry of the sea-bottom

between study area and the Drin River delta; arrows indicate transport

direction of the sand derived by the Drin River along the shore as

proposed by Babic et al. (2013). Note the very narrow shallow-marine

zone between Budva and Dubrovnik

846 Facies (2014) 60:843–863

123

submerged (Figs. 1, 2). Most of the modern terrestrial

material is supplied to the study area by two major riv-

ers, Cetina River on the north, and Neretva River on the

south, with sediment accumulation rates between 4 and

6 mm year-1 (Jurina et al. 2013).

The modern wind regime at the eastern Adriatic coast is

complex (as shown for the study area in Fig. 1). There are

several wind systems of different directions and velocities,

and the two strongest, the ‘‘bura’’ and ‘‘jugo’’, are blowing

throughout the year but their velocities are higher in winter.

The ‘‘bura’’ wind is a strong, cold, and mostly dry conti-

nental wind that blows from the northeast, i.e., from the

hinterland over the mountains and down their coastal

slopes to the Adriatic Sea, affecting also the islands,

reaching sometimes more than 60 m s-1. The wind is

channelized, strongly depending on topography, and is

commonly related to anticyclones. ‘‘Jugo’’ is a strong

cyclonic humid wind that blows from the southeast, i.e.,

parallel to the coast, affecting the islands. During storms,

the wind reaches velocities up to 30 m s-1, but its velocity

significantly decreases approaching the land.

Methods

Measurements of paleowind directions and mineralogical

analysis were undertaken in order to determine the wind

regime that operated on the coast, as well as possible source

areas during the late Pleistocene. The fieldwork comprised

detailed facies analysis and sampling for mineralogical and

paleontological analyses. The two-dimensional geometry of

sandy units and dimensions of sedimentary structures were

measured at outcrops, and the influence of biological activity,

such as traces of plant roots, was recorded. Foreset dip direc-

tions in cross-beds were measured in order to determine pa-

leowind directions. In order to interpret the depositional

mechanism of breccia units, clast-size, and geometry of the

body was measured, and the rounding and sorting of the clasts

and matrix were described.

The grain size of 19 sandy samples was analyzed by wet

sieving. Modal composition was performed on the

0.063–0.125-mm calcite-free fraction. Determination of the

calcium carbonate content was carried out by the Scheibler

standard method according to ONORM L 1084 (1989).

Fig. 3 Geological map of the study area (modified after FGI 1970) showing the complex lithological composition of the Karst Dinarides (only

Triassic rocks in the NE corner of the map belong to the Inner Dinarides). The studied locations are marked by black circles and bold lettering

Facies (2014) 60:843–863 847

123

Heavy and light mineral fractions (HMF and LMF) were

separated by bromoform liquid (CHBr3; d = 2.86 g cm-3).

Qualitative and quantitative analyses of HMF and LMF

were performed by identifying 300–350 grains per sample

under the polarization microscope (following method by

Mange and Maurer 1992). Composition of five weakly

cemented sandstone samples was determined by thin-sec-

tion image analysis under a polarization microscope.

Results

Mineralogical analysis

The sands are composed of carbonate and siliciclastic particles,

in most cases of terrigenous origin. They are very fine to

medium-grained, mostly very well to moderately well sorted,

with a near-symmetrical, either fine-skewed or coarse-skewed

Fig. 4 Microphotographs showing weakly cemented sands from the

studied localities. For the position of samples, see Figs. 5, 6, 8, 10,

and 11. The sample from Hvar is from Pavelic et al. (2011). The

composition of sands from Vis (a) and Hvar (b) is characterized by

the dominance of carbonate clasts derived from older limestones and

the absence of penecontemporaneous bioclasts. The sand from

Lastovo (c) is rich in penecontemporaneous shallow-marine bioclasts,

while more than two-thirds of particles originated from non-carbonate

rocks in sands from Korcula (d), Mljet (e), and Peljesac (f)

848 Facies (2014) 60:843–863

123

grain-size distribution (Figs. 4, 5, 6, 7, 8, 10, 11, 12). There are

remarkable differences in color and mineralogical composition

among aeolian sandy deposits on Vis and Hvar to the north and

Korcula, Lastovo, Mljet and Peljesac Peninsula to the south. A

relatively high content of CaCO3 defines most of the sand as

calcareous.

At Vis and Hvar the sands are mainly yellowish to light

brownish and generally contain 70–80 % CaCO3 (Figs. 5,

12). They are dominated by well-rounded rock fragments

of microsparitic, sparitic, and micritic limestones (Fig. 4a,

b). The siliciclastic grains make up around 20 % of all

particles, being dominated by rock fragments (mostly chert

and microquartzite, rarely quartzsericite schist) and quartz,

whereas feldspars and heavy minerals make up around

10 %. Among feldspars, plagioclase grains showing poly-

synthetic twinning and fresh orthoclase are observed. The

heavy mineral association (HMA) is dominated by trans-

lucent heavy minerals (THM) and opaque minerals. The

most common THM are amphiboles and pyroxenes, fol-

lowed by the epidote group and garnets (Table 1).

At Mljet, Korcula, Peljesac, and Lastovo, the sands

are brownish to dark brownish and in most cases

contain 15–50 % CaCO3 (Figs. 6, 7, 8, 10, 11). They

are composed of siliciclastic (50–80 %) and carbonate

(20–50 %) particles. Rock fragments (dominantly chert,

quartzite, and pyroclastic rocks, sporadically quartz-

sericite schist, and spilite), quartz grains and heavy

minerals are the most common siliciclastic particles. In

the HMA, the translucent heavy minerals (THM)

dominate (70–92 %), opaque minerals are significant

(7–27 %), and chlorite is considerably less abundant.

Pyroxenes are the most common THM while amphi-

boles are the second most common group (Table 1).

Carbonate particles at Korcula, Mljet and Peljesac

(Fig. 4d, f) consist of well-rounded fragments of mi-

crosparitic, micritic, and sparitic limestones with only a

few bioclasts of benthic foraminifera and molluscs. The

composition of the carbonate particles at Lastovo dif-

fers from all other localities, as they contain well-

rounded fragments of older limestones, but also a

significant amount of penecontemporaneous shallow-

marine carbonate bioclasts such as fragments of red

algae, benthic foraminifera, molluscs, and echinoids

(Fig. 4c).

Table 1 Modal composition of sands from the islands of Vis, Mljet, Lastovo, Korcula, Hvar, and the Peljesac Peninsula

Sample HMF

(%)

Heavy mineral fraction (HMF) (%) Light mineral

fraction (LMF) (%)

op ch dol thm Translucent heavy minerals (THM) q f rf ms

tu zr ru ap am opx cpx ep ga st tit ol csp x

Vis-I/1 9.53 40 1 ? 58 ? 3 1 ? 43 9 26 7 5 ? ? ? 2 2 43 8 49

Vis-I/2 7.71 34 1 1 64 1 ? 2 1 40 9 35 5 3 1 ? 2 39 10 51

Vis-I/3 13.03 58 ? 1 40 1 ? 1 1 36 12 32 7 6 1 ? ? 1 48 7 45

Vis-I/4 11.88 54 ? 1 44 2 2 1 ? 33 9 36 8 7 1 1 42 10 48

Hvar-I/1 5.12 60 ? 40 3 1 2 ? 54 3 14 9 10 ? ? 1 2 49 10 41 ?

Hvar-I/3 6.67 42 58 1 2 1 48 9 26 7 4 ? ? ? 1 54 3 42 1

Mlj-I/1 47.62 15 ? 84 ? 15 21 49 10 ? ? 1 2 1 33 3 64

Mlj-I/2 54.50 17 ? 82 11 25 51 9 ? 1 ? ? 2 33 2 65

Mlj-I/3 59.66 17 1 82 17 23 44 12 1 ? 1 1 31 3 66

Mlj-II/1 34.54 11 2 87 ? ? 23 23 38 12 ? ? 2 44 4 52

Mlj-II/2 60.93 15 ? 85 22 27 41 8 ? ? 1 25 1 74

Kor-I/1 26.99 7 2 2 91 40 16 27 11 2 – 1 3 26 6 68

Kor-I/2 25.95 10 2 ? 87 33 15 33 15 ? ? ? ? 2 24 3 73

Pelj-I/1 55.84 13 87 19 28 44 6 1 ? 2 26 2 72

Pelj-I/2 54.55 8 ? 92 23 26 42 7 – ? 2 26 3 71

Lst-I/1 51.62 12 88 12 32 44 9 ? ? ? 2 44 3 53

Lst-I/2 31.44 27 3 70 ? ? ? 20 25 36 12 1 ? 1 1 2 36 4 60

Lst-I/3 18.29 11 1 88 ? ? 22 24 38 12 ? ? ? 2 38 1 61

Lst-I/4 23.86 13 2 85 26 24 36 10 1 1 2 36 1 63

Op opaque minerals, ch chlorite, dol dolomite, thm translucent heavy minerals, tu tourmaline, zr zirconium, ru rutile, ap apatite, am amphibole,

opx orthopyroxene, cpx clinopyroxene, ep epidote, ga garnet, st staurolite, tit titanite, ol olivine, csp chromian spinel, x undetermined, q quartz,

f feldspar, rf rock fragments, ms muscovite

Facies (2014) 60:843–863 849

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850 Facies (2014) 60:843–863

123

Facies and vertical facies associations

The sand bodies are composed of cross-bedded co-sets that

can be followed laterally over several tens of meters on some

localities. The bodies are characterized by a variety of foreset

dip directions. Subordinate horizontally bedded sandy units

also occur. The sands are intercalated with breccia lenses in

some places. Most of the deposits belong to five main

facies––two interpreted as aeolian, and three as alluvial

deposits (Table 2).

Vis

The outcrop studied at Vis (Figs. 1, 3) is located in a

shallow NE–SW elongated valley. It is represented by a

140-m-long sand pit of irregular curved shape in plan view,

oriented SE–NW, with the base at 117 m a.s.l. The sand

body is more than 10 m thick, but due to sand slides, only

the upper and occasionally middle parts of the vertical

exposure were available for study (Fig. 5). The body is

composed of a sub-horizontally laminated unit separated

by a sharp bounding surface from an overlying cross-

bedded unit (Table 2).

Sub-horizontally laminated sand crops out at the base of

the southern part of the profile (Fig. 5c, lower part). The

visible thickness of this unit is 50 cm but its lateral extent

is unknown due to a cover of weathered sand. The lami-

nation has a primary dip of 1–5� with a mean direction to

the NNW. The unit probably represents a bottomset of the

aeolian dune (Table 2).

The cross-bedded unit is up to 9.5 m thick and can be

traced along the whole profile (Table 2; Fig. 5b, c). The upper

part of the unit is eroded, so the original thickness is not

known. The foresets dip is unimodal with mean direction

towards 340�, i.e., towards the NNW (Fig. 5). Within less

steep dune foresets, rare isolated cross-laminated intrasets

occur. The unit is interpreted as an aeolian dune (Table 2).

The intrasets may represent faster migrating secondary bed-

forms such as small dunes or ripples developed on the slopes

of a large, primary bedform (cf. Hunter 1977; Kocurek 1991;

Mountney and Thompson 2002).

Mljet

The sandy deposits of Mljet were studied in a small shal-

low valley striking NE–SW. Two adjacent sections were

measured, Mljet-I and Mljet-II (Figs. 1, 3). Mljet-I is

exposed in a small profile, 7 m long and 4.2 m high

(Fig. 6). The base of the section is located at about 16 m

a.s.l. At Mljet-II, only a 10-m-thick succession was

Fig. 5 Sketch of the Vis-I outcrop showing aeolian deposits, their

grain-size distribution, CaCO3 content, and paleocurrent rose dia-

gram. a In the middle of the photograph, a small isolated set of cross-

laminated sand within foresets is visible. b Sub-horizontally

laminated sands, separated by a major bounding surface marked by

the dotted line (lower part; hammer is 31 cm long). c The aeolian

deposits are mostly represented by cross-bedded sands with well-

defined foresets. For position of the section, see Figs. 1 and 3

Facies (2014) 60:843–863 851

123

measured because the outcrop is covered by sand slides and

vegetation, and the lateral extent of sedimentary units is not

known (Fig. 7). The succession at Mljet-I overlaps with the

basal part of the succession at Mljet-II. Cross-bedded and

horizontally bedded sandy units prevail, but breccia units

also occur.

Horizontally bedded sands compose units that vary in

thickness between 10 and 150 cm. Some thicker units show

horizontal bedding with strata a few centimeters thick

(Figs. 6, 7). Scattered and isolated limestone clasts occur

within some units, drawing a faint horizontal stratification.

Sands are mainly brownish, some reddish, and the unit at the

base of Mljet-II shows reddish-brown color mottling. The

sand is interpreted as sheet flow deposits, whereas the reddish

color and mottling indicates that sand underwent pedogenic

processes (Table 2). The isolated limestone clasts are inter-

preted as rolling and rockfall clasts transported down the

slope from W.

Sets of cross-bedded sands vary in thickness between

90 and 160 cm (Figs. 6, 7; Table 2). The cross-bedded

units overlie the breccia and horizontally bedded sand by

a distinct horizontal surface. In the lower portion of

Mljet-II, two sets separated by a bounding surface form a

co-set (Fig. 7). Foresets are medium- to high-angle pla-

nar or tangential. At Mljet-I the dip azimuths of foresets

are towards a mean direction of 198�, i.e., towards the

SSW (Fig. 6). At Mljet-II, the mean direction is 139�,

towards the SE (Fig. 7). Some small isolated cross-lam-

inated sets occur within the cross-bedded sands. Rare

fragments of terrestrial gastropods were found in the

cross-bedded unit in the middle part of the Mljet-I sec-

tion. The cross-bedded sands are interpreted as repre-

senting aeolian dunes and small isolated cross-laminated

sets probably represent small secondary dunes or ripples

(Table 2). The bounding surface within the co-set

(Fig. 7) was probably formed by wind erosion due to

dune migration in the downwind direction and sub-

sequent reactivation (cf. Kocurek 1991).

Low-angle cross-bedded sands form isolated sets 40 to

200 cm thick (Figs. 6, 7). The foresets dip angle is 2–8�with a mean direction of 160�, i.e., towards the SSE. They

are interpreted as representing a sand sheet (Table 2).

Breccias form irregular lens-shaped units that lie in

scours or channels up to 60 cm deep. They also occur as

thin sheets within various types of sand in places (Figs. 6,

7; Table 2). Channel or scour axes are oriented 70� and

110�. The breccia probably represents alluvial channel

deposits, while thin sheet-like bodies are interpreted as

being deposited from sheet flows (Table 2). The nature of

the breccias characteristics indicate a short transport and

the orientation of the channel or scour axes suggests source

from nearby hills situated towards WNW.

Fig. 6 Aeolian and alluvial deposits at Mljet-I, their grain-size

characteristics, CaCO3 content, and paleocurrent rose diagram. The

aeolian deposits are represented by a cross-bedded unit in the central

part of the outcrop. The unit is partly eroded by a channelized breccia

visible at the right side of the outcrop. The cross-bedded unit and the

breccia lenses are overlain by a relatively thin low-angle cross-bedded

unit. Horizontally bedded sandy units with scattered, locally derived

limestone clasts can be seen in the lowermost and uppermost parts.

The cross-bedded sandy units are separated from the horizontally

bedded sandy units by major bounding surfaces (dotted lines).

Hammer is 31 cm long. For position of the section, see Figs. 1 and 3

852 Facies (2014) 60:843–863

123

Lastovo

Sands at Lastovo occur in a shallow E–W elongated valley,

and are exposed along the northern wall of a sand pit with

the base at about 38 m a.s.l. (Fig. 8). Two depositional

units are distinguished: a horizontally bedded sandy unit,

overlain by a cross-bedded sandy unit.

The horizontally bedded unit is 2.9 m thick and consists

of intercalated beds of different colors (sheet flow sands in

Table 2 and Fig. 8c). The bed boundaries are gradational.

Irregular non-lithified caliche nodules roughly outline the

stratification of the brown sand. Dispersed whole shells and

fragments of terrestrial gastropods are fairly abundant in

the unit (Fig. 8b), and in places highly concentrated. They

are represented by two species, Xerolenta obvia and

Chondrula tridens (Fig. 9). The sands are interpreted as

deposited from sheet flows (Table 2), and they were tem-

porarily affected by pedogenesis in a warm climate, as

indicated by the paleoecology of the gastropods (Lozek

1964; Frank 2006). The irregular non-lithified caliche

nodules indicate water-table fluctuations.

The original thickness of the cross-bedded sandy unit

is not known, due to the modern truncation but pre-

served thickness reaches a maximum of 1.4 m. The base

is a sharp surface that separates the cross-bedded unit

from the horizontally bedded sandy unit (Fig. 8a).

Within the upper unit, low-angle planar bounding

surfaces sharply truncate the foresets separating smaller,

35–60-cm-thick sets. The surfaces dip towards the west.

The foresets dip between 5� and 15�, and the mean dip

direction is 265�, i.e., towards the west, similar to the

planar bounding surfaces (Fig. 8). The unit is inter-

preted as representing a sand sheet, where the low-angle

bounding surfaces were probably produced by super-

imposed bedform migration (Table 2). Rare small-scale

channel-like breccia lenses occur within the cross-bed-

ded unit interpreted as being deposited from high-con-

centration sediment flows (Table 2).

Korcula

At Korcula, a 43-m-long profile is exposed in a topographic

saddle striking N–S. It is a single sandy unit (Fig. 10) with

the base at about 10 m a.s.l. The maximum visible thick-

ness of the unit is only 2 m due to sand slides and modern

erosion. The unit is cross-bedded, and the foresets dip is

mostly 26–36�, and the average dip directions are towards

327�, i.e., to the NW (Fig. 10). The unit is interpreted as

representing an aeolian dune (Table 2).

Peljesac

A small patch of fine-grained and very well sorted sand

covers the lowermost part of the slope of a steep hill at the

Fig. 7 Section Mljet-II showing the stratigraphic profile with inter-

calation of aeolian and alluvial deposits, their grain-size character-

istics, CaCO3 content, and paleocurrent rose diagram. The succession

is characterized by intercalation of aeolian cross-bedded sandy units,

and alluvial horizontally bedded sandy units and breccia lenses. For

position of the section see Figs. 1 and 3

Facies (2014) 60:843–863 853

123

southeastern-most part of the Peljesac Peninsula (the top of

the hill is at 282 m a.s.l.). A section through a 31-m-long

profile was measured in a road cut at about 18 m a.s.l.

(Fig. 11). It is a sandy unit, 7 m thick, which shows a

planar-stratification and planar-lamination (Fig. 11). The

beds and laminae are moderately to steeply inclined

(18–34�) with the mean dip direction of 256�, i.e., down-

hill. The sand is interpreted as a sheet flow deposit on the

hill slope (Table 2). The interpretation is supported by the

uniform grain size and the planar stratification and planar

lamination inclined downhill that indicates aeolian sand

erosion during periods of intense rainfall and deposition in

a small-scale alluvial fan (Sweeney and Loope 2001).

Hvar

Sands are found at several localities at the island of

Hvar (Markovic-Marjanovic 1976) and have been

Fig. 8 Sketch of the outcrop at Lastovo-I section showing aeolian

and alluvial deposits, their grain-size characteristics, CaCO3 content,

and paleocurrent rose diagram. a Aeolian deposits represented by

cross-bedded sands in the uppermost part of the cross section are

laterally extensive. b Terrestrial gastropods occurring within

horizontally bedded sands, which are characterized by intercalations

of light brown and reddish brown layers indicating pedogenesis (c).

The cross-bedded sandy unit overlies the horizontally bedded sandy

unit. Scale is 2 m long. For position of the section, see Figs. 1 and 3

Fig. 9 Pleistocene terrestrial gastropods from Lastovo-I section. a, b, c Xerolenta obvia, sample Lst-I/1. d, e Chondrula tridens, sample Lst-I/2.

For position of samples see Fig. 8

854 Facies (2014) 60:843–863

123

described in detail and interpreted as aeolian at the

Sveti Mihovil locality (Pavelic et al. 2011). At Hvar-I

(Figs. 1, 3), sands and breccia form a 4.5-m-thick suc-

cession, which has not been previously studied. Three

breccia units occur in the succession (Fig. 12). They are

strongly erosional and mainly sheet-like, but rest in

deep scours in places (Table 2). The units are composed

of amalgamated beds, several centimeters to a few

decimeters thick, which can be distinguished by a var-

iable sandy matrix content and a bimodal clast-size

distribution. The breccias are matrix- to clast-supported,

but a matrix is completely lacking in some beds. The

clasts are composed of Lower Cretaceous carbonates.

The breccias were deposited by powerful flows

(Table 2). The variable matrix content, bimodal matrix

grain sizes, clast segregation, and amalgamated beds are

probably a consequence of multi-storey accumulation in

an alluvial environment (Steel and Thompson 1983).

The clast size, angularity, and composition reflect short

transport from nearby hills.

Thin isolated lenticular sand bodies occur within the

breccia units. They were deposited by lower velocity cur-

rents including additional source of material, probably

aeolian sand, as indicated by mineralogical composition.

The sands separating breccia bodies form two horizon-

tally bedded units showing a gradual transition from

underlying breccia units and erosional and scoured top

surfaces giving the sandy units irregular lateral geometry.

The sands were probably deposited from sheet flows

(Table 2).

Fig. 10 Sketch and photograph of Korcula-I section, showing aeolian sands, their grain-size characteristics, CaCO3 content, and paleocurrent

rose diagram. For position of the section, see Figs. 1 and 3

Facies (2014) 60:843–863 855

123

Discussion

Provenance of the sands

The modal composition shows that the studied late Pleis-

tocene sandy deposits originated from erosion of various

rock types. The dominance of chemically unstable detritus

such as limestone fragments, carbonate bioclasts, pyrox-

enes, and amphiboles indicates that sediments are miner-

alogically immature. Such sediments are most commonly

produced under arid climate conditions. Occasionally, they

could have resulted from a very short transport, but tex-

tural maturity of the studied sands, indicated by good

sorting and well-rounded grains, suggests either a rela-

tively long transport of material or several cycles of

reworking.

There is a remarkable difference in the mineralogical

composition between aeolian sandy deposits at Vis and

Hvar in the north and Korcula, Lastovo, Mljet, and Peljesac

in the south, as indicated by the ratio between carbonate

and siliciclastic clasts, differences in composition of silic-

iclastic detritus, and sand color. The predominance of

limestone fragments indicates that subaerially exposed

older limestones were the major source for the calcareous

sands at Vis and Hvar. A significant content of carbonates

was also found in the calcareous sand at Lastovo, but this is

Fig. 11 Photograph of Peljesac-I section showing alluvial downhill

inclined plane-stratified more or less cemented sands, their grain-size

characteristics, and CaCO3 content. For position of the outcrop, see

Figs. 1 and 3

Fig. 12 Sketch and photograph of the outcrop at the Hvar-I locality showing intercalation of alluvial horizontally bedded sandy units and breccia

units with erosional base. For position of the outcrop, see Figs. 1 and 3

856 Facies (2014) 60:843–863

123

primarily caused by a high content of penecontemporane-

ous shallow-marine bioclasts. Sandy deposits at Mljet,

Korcula, and Peljesac contain between 66 and 80 % par-

ticles of non-carbonate rocks, and at other localities their

content varies between 20 and 60 %. Microquartzite,

quartzite, and quartzsericite schist clasts were derived from

metamorphic rocks, while pyroxenes, amphiboles, epidote,

garnets, and titanite could have been produced by weath-

ering of various metamorphic and magmatic rocks. Minor

presence of chrome spinel and olivine in most of the sands

indicate an ultramafic magmatic source, while part of the

quartz grains, plagioclase with polysynthetic lamellae, and

alkali feldspars were probably derived from acidic mag-

matic rocks. Tephra fragments as well as very fresh green

clinopyroxenes (augite) in sands at Mljet, Korcula, and

Peljesac are probably products of the Quaternary volca-

nism (Lugovic et al. 2006; Mikulcic Pavlakovic et al. 2011;

Wacha et al. 2011b; Babic et al. 2012). The presence of

chert rock fragments and rounded quartz grains in all sands,

and of the ultra-stable translucent heavy minerals tourma-

line, rutile, and zircon in sands at Vis and Hvar indicate

that part of the detritus was produced by recycling of older

sedimentary rocks.

The source area of siliciclastic, carbonate clastic and

bioclastic detrital sands had to be lithologically complex.

The siliciclastic and carbonate clastic detritus was most

probably released by breakdown of sedimentary, igneous,

and metamorphic rocks in the Dinarides that are composed

of different, mostly carbonate rocks (Karst Dinarides), and

siliciclastic sedimentary rocks, magmatic and metamorphic

rocks (Inner Dinarides). During the Late Pleistocene gla-

ciations, glaciers formed within the Dinarides (Bognar and

Prugovecki 1997; Marjanac and Marjanac 2004; Hughes

et al. 2011; Velic et al. 2011) that probably caused strong

erosion, and the products were transported by local rivers to

the coastal area during seasons characterized by warm cli-

mate. Huge amounts of sand deposited in river channels and

on flood plains were later reworked by wind, generating

aeolian deposits at the coast under drier and cooler condi-

tions (Bognar et al. 1992; Pavelic et al. 2011; Babic et al.

2012, 2013). This interpretation can be partly compared to

the Pleistocene Ebro Basin in Spain, where an outwash

plain was deflated generating aeolian sand deposition (Lu-

zon et al. 2012). Additional sand provenances may be from

numerous small Pleistocene alluvial cones composed of

sands and sandstones in the lower parts, and breccias in the

upper parts. They developed locally along steep slopes of

the eastern Adriatic coastal hills and mountains, whose

distal zones might have been flooded during the Holocene

sea-level rise (Borovic et al. 1977; Marincic et al. 1977;

Magas et al. 1979).

Penecontemporaneous shallow-marine biogenic grains

represent an important calcareous component of the aeolian

sand only in Lastovo section (Table 3). The occurrence of

penecontemporaneous marine bioclasts and foraminifera in

aeolian sand has also been observed on other mid-Adriatic

islands (Babic et al. 2012, 2013), but in very small

amounts, even on Korcula and Vis where aeolian deposi-

tion was controlled by landward-blowing winds that could

have potentially caused significant deflation of shallow-

marine bioclastic material. This suggests that deflated

shallow-marine sands did not play an important role in

producing of clastic detritus except in the case of Lastovo,

where the drift of marine sand probably increased due to

wind approaching oblique to parallel to the coast (Table 3)

(Hesp 1983).

The position of the modern Cetina and Neretva Rivers,

which supply the mid-Adriatic coast with material derived

from the Dinaric Mountains, allows interpretation of the

different mineralogical compositions between the northern

and southern localities (Fig. 3 and Table 2). The northerly

located Cetina River flows through the Karst Dinarides,

which are mostly composed of carbonates, including

Miocene lacustrine carbonates in the hinterland (de Leeuw

et al. 2010, 2012). If such a river existed in the Late

Pleistocene it probably supplied the coastal area with sand

produced by glacial processes in the mountains, passing

into wide flood plains towards the sea. This reconstruction

suggests that yellowish to light-brownish calcareous-rich

aeolian deposits at Hvar and Vis were probably generated

Table 3 Summarized major

characteristics of aeolian sands

studied

Data for the island of Hvar are

from this study and Pavelic

et al. (2011). Maximal altitude

from Mljet after Markovic-

Marjanovic (1979)

Locality CaCO3

content

Bioclasts

occurrence

Prevailing source

material

Bedforms Wind direction Max. altitude

m a.s.l.

Vis 74–80 No Limestones Dune Landward 125

Hvar 62–96 No Limestones Dunes, sand sheets Seaward 84

Mljet 15–32 Rare Metamorphics,

magmatics

Dunes, sand sheets Seaward 200

Lastovo 25–58 Common Biogenic,

metamorphics,

magmatics

Dunes Parallel to the

coastline

46.5

Korcula 28–35 Rare Metamorphics,

magmatics

Dune Landward 12

Facies (2014) 60:843–863 857

123

by deflation of the Cetina paleo-river deposits (Pavelic

et al. 2011). Brownish to dark-brownish sands at Korcula,

Lastovo, Mljet, and Peljesac, rich in siliciclastic material,

can be related to the southerly located Neretva River

(Buljan et al. 2012) (Fig. 3), with a headwater drainage

system situated in the Inner Dinarides that are composed

mostly of magmatic, metamorphic, and siliciclastic sedi-

mentary rocks (Fig. 3). The different mineralogical com-

position of the two groups of coastal aeolian sands may

thus be explained by the presence of two independent

fluvial systems with drainage in areas characterized by

different lithologies. Additionally, the different mineral-

ogical composition may also have been caused by exotic

material transported by glaciers from distant parts of the

Dinarides.

This interpretation differs from that of Babic et al.

(2013), who suggested a marine origin of most of the

aeolian sand and indicated that a transport towards mid-

Adriatic islands was by presumed strong marine currents

and waves alongshore from the SE reinforced by wind in

the late Pleistocene. As a major source of siliciclastic sand

for Korcula, Lastovo, Mljet, and Peljesac, they suggested

the Albanian coast where the large Drin River enters the

Adriatic Sea. According to Babic et al. (2013), the sand

was transported further towards the NW along the Mon-

tenegrian and Croatian coasts where it was subsequently

uplifted and reworked by wind action. However, the

modern bathymetric map documents a more than 50-km-

long very narrow and relatively steep nearshore fringe in

the Budva–Dubrovnik zone (Fig. 2b), which could not

have been passed by such a large amount of sand needed

for deposition in the study area. Moreover, the coastline

was located more seaward during lowstands, in the position

where the nearshore fringe was even steeper, additionally

reducing the sand passing capacity. This indicates that most

of the riverine material was deposited in the deltaic zones

without significant along-shore redistribution by marine

processes, and that deposition was predominantly con-

trolled by progradation and retrogradation of the coastline

due to the glacio-eustatic sea-level changes. Additionally,

strong and unidirectional longshore currents capable of

significant redistribution of river-derived material form

asymmetric or deflected wave-influenced deltas where the

river mouth runs subparallel to the coast (Wright 1977;

Bhattacharya and Giosan 2003), while the Drin River delta

is characterized by a symmetric morphology.

Wind regime and paleogeography

Transport directions of the aeolian sands show the pre-

vailing wind direction responsible for the formation and

migration of the aeolian dunes and sand sheets. Each

locality studied represented by the aeolian sands showed a

uniform wind direction with a spread in foreset dip direc-

tions mostly within 45�. However, comparison of these

directions shows a non-uniform and irregular wind regime

in the area (Fig. 13). Hvar (Pavelic et al. 2011) and Las-

tovo indicate westward wind directions, with a subordinate

southward deviation at Hvar. Vis and Korcula are charac-

terized by a north–northwestward transport direction. Mljet

differs from other localities, showing directions towards

the south-southwest and southeast, i.e., overall towards the

south. Reconstruction of the paleocoastline position based

on the modern bathymetric data and last maximal sea-level

drop of 120 m during the last glacial maximum (Corr-

eggiari et al. 1996) indicates that the localities studied were

part of the mainland at the time of sand deposition (Fig. 3).

The main aeolian bedforms show three general wind

directions: (1) landward at Vis and Korcula, (2) seaward at

Hvar and Mljet, and (3) parallel to the coastline at Lastovo

(Fig. 13, Table 3) that is similar to the modern wind

regime (Fig. 1).

If a wind regime similar to the modern wind regime

(Fig. 1) was active during the time of sand deposition on

the mid-Adriatic islands and Peljesac Peninsula, it is pos-

sible to relate these paleowind systems to deposits only

partly, because reconstructed wind directions mostly cor-

respond to the strike of the valleys or topographic saddles

as the sand depocenters. On Hvar, the eastern wind cor-

responds to the E–W elongated valley probably repre-

senting a deviated NE ‘‘paleo-bura’’ wind (Fig. 13). The

‘‘paleo-bura’’ probably controlled deposition on Mljet, too,

where the NE wind coincides with the NE–SW strike of the

saddle. The SE wind on Korcula partly corresponds to the

N–S-oriented saddle, while the eastern wind on Lastovo

corresponds to the E–W elongated valley, indicating

deviation of the SE ‘‘paleo-jugo’’ wind. The topography

did not affect the wind in the E–W valley on Vis where the

NNW wind direction reflects an influence of the ‘‘paleo–

jugo’’. Such wind deviations indicate that aeolian deposi-

tion at the coast was strongly controlled by local topogra-

phy characterized by a steep relief. Despite deviations, the

wind was still very strong, causing aeolian deposition at

very high altitudes: on Hvar up to 84 m and at Mljet up to

200 m a.s.l. (Markovic-Marjanovic 1979) (Table 3).

The wind directions that controlled aeolian deposition

on the mid-Adriatic islands differ strongly from most

Quaternary localities studied at other Mediterranean coasts,

where the dominant wind blew landward at most places,

such as the coasts of Mallorca (Clemmensen et al. 1997;

Nielsen et al. 2004), Sardinia (Andreucci et al. 2006, 2009),

Tunisia (Elmejdoub et al. 2011; Hasler et al. 2012), Egypt

(Frihy et al. 1988; El Banna 2004), and Israel (Yaalon and

Laronne 1971). This can be interpreted by their geographic

position within the Mediterranean realm, i.e., the influence

of the dominant wind that blew from the large open sea

858 Facies (2014) 60:843–863

123

towards coastal areas. Aeolian deposition was forced

especially during low stands when wide surfaces of sub-

aerially exposed marine beach sands were deflated by

onshore-blowing winds and the sand was subsequently

deposited on the backshore, resulting in a significant per-

centage of marine bioclasts. Aeolian deposition on the mid-

Adriatic islands was generated mainly by the wind that

blew more or less parallel to the coast as a consequence of

the narrow and NW–SE elongated semi-closed Adriatic

Sea, and by the wind that blew seaward. However, due to

the morphology of the islands that corresponds to the

geological structures and to the orientation of karst

depressions where the aeolian sand accumulated, it caused

local wind deviation in different directions. A remarkable

difference between aeolian sand at mid-Adriatic and

Mediterranean localities is also the mineralogical compo-

sition. The Mediterranean coastal aeolian sand is mostly

rich in marine bioclasts as the result of beach sand defla-

tion, while the sand on the mid-Adriatic islands is char-

acterized by relatively low content of bioclasts, as the

predominant source of sands were river flood plains where

material derived from the hinterland was deposited.

The existence of aeolian sands with marine bioclasts in the

proximity of the supposed paleo-coastline may define them

as coastal (Figs. 1, 13). However, a sequence of events

indicates inland dunes that have been formed by several

phases: (1) mechanical weathering of sand source, probably

by ice, (2) glacial and fluvial transport and deposition, (3)

aeolian transport and deposition, and (4) influence of land-

ward-blowing winds, corresponding to case 3 of Pye and

Tsoar (2009). This interpretation is supported by the complex

wind regime, including seaward-blowing winds.

Late Pleistocene deposition along the mid-Adriatic coast

was characterized by alternation of two phases. The aeolian

phase was characterized by deflation and reworking of flu-

vial sand seasonally supplied by rivers from the Dinarides

along the coast, by a complex wind regime partly controlled

by the local topography during a dry and cold climate

(Fig. 14a). The sand constructed dunes and sand sheets that

migrated in different directions across the land. Marine sand

was of minor importance as a source. A change to a wetter

and warmer climate resulted in an alluvial phase charac-

terized by a marked change in depositional style (Fig. 14b).

Small alluvial systems developed producing accumulations

of locally derived coarse-grained material and recycled

aeolian sand. Reduced wind influence caused stabilization of

aeolian bedforms, supported by vegetation and water-table

fluctuation, which colored the sand reddish and produced

Fig. 13 Schematic representation of the late Pleistocene paleogeog-

raphy of the study area showing wind directions and migrating dunes

in the area of the mid-Adriatic islands and Peljesac Peninsula, which

represented a part of the mainland during sea-level lowstands. Winds

blew towards the north–northwest, west and south, or landward,

seaward, and parallel to the approximated paleo-coastline. For

position of the area, see Fig. 1

Facies (2014) 60:843–863 859

123

Fig. 14 Depositional model for alternation of aeolian and alluvial

phases on the mid-Adriatic coast during the late Pleistocene related to

the alteration of dry and cold glacial and wet and warm interglacial

stages. a Deposition during the aeolian phase was characterized by a

strong seasonal sediment supply by rivers and dune and sand sheet

migration. Local wind deviation caused by morphology generated the

aeolian deposition in the karst depression. b During the alluvial phase,

erosion caused weathering of basement rocks and deposition of

produced fragments together with recycled aeolian sand deposited in

locally developed alluvial systems. The sediment supply by rivers was

low and the flood plain was affected by pedogenesis. Aeolian

bedforms were stabilized by increased humidity and vegetation in

places. c During the subsequent aeolian phase, the flood plain was

deflated by wind that constructed sand into dunes and sand sheets

860 Facies (2014) 60:843–863

123

caliche nodules by pedogenesis. The change to a drier,

colder, and windier climate triggered evolution of a new

aeolian phase (Fig. 14c). Deflation of sand previously

deposited on the flood plain, together with the new sea-

sonally supplied fluvial sand and a minor contribution of

marine sand exposed on the surface due to the sea-level fall,

resulted in the formation of a new generation of dunes and

sand sheets. Mobilization of the aeolian bedforms was

additionally supported by disappearance of vegetation and

water-table fall due to a sea-level fall. These phases could be

related to the alternation of dry and cold glacial and wet and

warm interglacial stages.

Conclusions

1. Late Pleistocene coastal aeolian and alluvial deposition

on the mid-Adriatic islands of Hvar, Vis, Lastovo,

Korcula, and Mljet, and the Peljesac Peninsula was

controlled by multiple factors.

2. Glacial processes in the Dinaridic mountains caused

mechanical weathering of different types of rocks and

high production of sand-sized particles.

3. The main source of the aeolian bedforms was material

produced by mechanical weathering in the Dinarides

that was transported to the coastal belt by paleo-Cetina

and paleo-Neretva Rivers during periods when the

mid-Adriatic islands were part of the mainland due to

the glacio-eustatic sea-level falls. The marine sand

contributed variable, but mostly relatively small

amounts of marine bioclasts to the aeolian sand.

4. During glacial periods and resulting sea-level falls the

flood plains and marine sands were deflated, resulting

in accumulation of sand in aeolian bedforms by a

complex wind regime characterized by wind direction

deviations in basins controlled by the morphology of

the islands that mostly corresponds to the geological

structures and orientation of karst depressions. The

wind regime differs from most coastal aeolian envi-

ronments in the Mediterranean realm, which are

predominantly characterized by landward winds.

5. Frequent climate changes resulted in alternations of

predominantly aeolian and alluvial deposits probably

related to the alternation of dry and cold glacial and

wet and warm interglacial stages.

Acknowledgments Antun Husinec (St. Lawrence University, USA)

and Ana Maricic (University of Zagreb) are gratefully acknowledged

for their assistance in the fieldwork, Adriano Banak (Croatian Geo-

logical Survey) for providing some of the field photographs from Vis,

and Alica Bajic (Croatian Meteorological and Hydrological Service)

for providing data on modern wind directions. The review of an early

version of the manuscript by Finn Surlyk (University of Copenhagen)

is gratefully acknowledged. The authors would like to thank journal

editor Franz Fursich, Aranzazu Luzon (University of Zaragoza), and

an anonymous reviewer for their helpful comments. The study was

supported by the Ministry of Science, Education and Sports of the

Republic of Croatia through projects Nos. 195-1951293-2703, 195-

1951293-0237, 119-1191155-1159, 195-1953068-0242, 195-1953068-

2704 and 181-1811096-1093.

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