Pleistocene and Holocene aeolian sediments of different location and geological history: A new...

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Quaternary International xxx (2013) 1e12

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Pleistocene and Holocene aeolian sediments of different location andgeological history: A new insight from rounding and frosting of quartzgrains

Edyta Kali�nska a, *, M�aris Narti�ss b

a Institute of Ecology and Earth Sciences, Department of Geology, Faculty of Science, University of Tartu, Ravila Str. 14A, Tartu EE50411, Estoniab Faculty of Geography and Earth Sciences, University of Latvia, Alberta Str. 10, Riga LV1586, Latvia

a r t i c l e i n f o

Article history:Available online xxx

* Corresponding author.E-mail address: [email protected] (E. Kali�nska)

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a b s t r a c t

Rounding and frosting of quartz grains in aeolian sediments of the known stratigraphic position andunique geological setting was explored in Finnish, Estonian, Latvian, and Polish localities and in Fuer-teventura Island. The aim of the study is to characterize the variability of the spatial pattern of roundingand frosting of quartz grains in the sandy (0.5e0.8 mm) fraction and to evaluate the factors influencing it.The relationships between rounded and non-abraded, as well as matt- and shiny-type quartz grains werecalculated for 159 samples and evaluated against the aeolian subenvironment, substratum and presumedage of the locations. The obtained relations do not confirm meridional changeability of textural featurespreviously observed in Poland and suggest a larger impact of the substratum on textural features of cold-environment aeolian sediments.

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1. Introduction

The shape and surface features of quartz grains of the sandfraction can provide important information about the character ofprocesses responsible for sediment deposition (Krinsley andDoornkamp, 1973; Velichko and Timirieva, 1995; Mahanay, 2002;Velichko et al., 2009). The correlation of selected textural fea-tures, such as grain-size distribution (Mycielska-Dowgia11o andLudwikowska-Kedzia, 2011), rounding and frosting of quartzgrains in the sand fraction (0.5e0.8 mm) (Mycielska-Dowgia11o andWoronko, 2004) and mineral-petrographic composition (Barczukand Mycielska-Dowgia11o, 2001) of sediments, can shed light onthe transport behaviour, and size-sorting of sediments in variousenvironments (Folk and Ward, 1957; Anthony and Héquette, 2007;Flemming, 2007; Mycielska-Dowgia11o and Ludwikowska-Kedzia,2011), and the duration of aeolian processes (Mycielska-Dowgia11o, 1993). The aim of this study is to explore the differ-ences in the formation of aeolian deposits sampled in differentparts of Europe (Fig. 1) explored by a complex approach of patternsof textural features, rounding and frosting of quartz grains inparticular. The study comprises the following steps: (1) analysis ofrounding and frosting of quartz grains in the sand (0.5e0.8 mm)

.

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, E., Narti�ss, M., Pleistocene aand frosting of quartz gr

fraction according to the methodology by Cailleux (1942), modifiedafter Mycielska-Dowgia11o and Woronko (1998); (2) calculation ofcoefficients between rounded and non-abraded, as well as matt-and shiny-type quartz grains; (3) enlightening the clusters under (i)geographical position of the sites; (ii) subenvironment; (iii)geological setting and substratum of aeolian sediments in partic-ular; (iv) age of aeolian sediments. Samples from five locations:NNE Fuerteventura Island, Central Poland, E Latvia, NE Estonia, andW Finland (Fig. 1) were examined, representing different meridi-onal, climatic and geological conditions. All sites except Fuerte-ventura Island belong to “the European Sand Belt” (Zeeberg, 1998).

2. Geological and geomorphological settings of the locations

2.1. Fuerteventura

The Corralejo dune field (Fig. 2A) is located in the NNE part ofFuerteventura Island, on a raised beach that covers a shore platformon Miocene lavas (Gutiérrez-Elorza et al., 2011). It is formed by aprevalence of aeolian sheets, less than 10 m thick (Lancaster, 1995)both in the north and in the south, and abounds in groups ofw10mhigh transverse dunes with steep slip faces in the central part(Criado and Hansen, 2000; Criado et al., 2004). In an elliptic blow-out in the central part the dune field, a cemented sandy level rich interrestrial gastropoda has yielded ages ranging from 13,890 � 110to 16,980 � 120 cal. BP (Criado and Hansen, 2000).

nd Holocene aeolian sediments of different location and geologicalains, Quaternary International (2013), http://dx.doi.org/10.1016/

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Fig. 1. Location of the investigated sites (LGM refers to the Last Glacial Maximum). In grey e the extent of the “European Sand Belt” according to Zeeberg (1998).

E. Kali�nska, M. Narti�ss / Quaternary International xxx (2013) 1e122

2.2. Central Poland

The aeolian sediments of Central Poland belong to the centralpart of the “European Sand Belt” (Zeeberg, 1998) in the foreland ofthemaximal extent of theWeichselian (Vistulian) glaciation (Marks,2012). Sandy aeolian sediments (Jaktorów, Ko1aczek and Plecewicesites e Fig. 2BeD, respectively) cover the northern margin of theWarsaw Basin, surrounding a plateau built of morainic tills of theSaale (Warthanian) glaciation, andglaciolacustrine varved clays thataccumulated at least during two glacial episodes in the WarsawBasin: the Saale (Warthanian) and Weichselian (Vistulian) glacia-tions (Marks, 2005, 2012). The sandy zonewas developedduring thelatter (Vistulian,Weichselian) glaciation in four episodes: 48e39 ka,the Grudziadz Interstadial in Poland (Drozdowski and Fedorowicz,1987); 28e25 ka before the Last Glacial Maximum (LGM); 16e14 ka, the Pomeranian Phase and the Younger Dryas about 12 ka(Kali�nska, 2008, 2010). The rare dunes (Miedzyborów site, Fig. 2E),whichoverlie the coversand, areparabolic in shape, up to fewmetreshigh and their age is correlated with Late Glacial time. The radio-carbon dating of palaeosols, found within the dunes profile in theWarsaw Basin, yielded the ages of 13,340 � 110 to 12,770 � 130 BP,12,150� 270 BP, 12,030� 170 BP, 11,150� 130 BP, and 10,400� 450BP (Konecka-Betley and Janowska, 2005).

2.3. Eastern Latvia

The Majaks site (Fig. 2F) is located in the southern part of theEastern Latvian lowland. Aeolian landforms lie on top of sandyglaciolacustrine sediments deposited in the Nicgale ice-dammedlake. The Nicgale ice-dammed lake formed in front of the retreat-ing Lubans ice lobe after the Gulbene (Middle Lithuanian) degla-ciation phase of the Late Weichselian ice sheet (Zel�cs and Markots,2004). North of Daugavpils (25 km southeast of the Majaks site),sandy glaciolacustrine sediments dated by OSL have yielded an ageof 14.5e15.5 ka (Zel�cs et al., 2011), thus setting the maximal agelimit of any aeolian activity at the Majaks site.

Please cite this article in press as: Kali�nska, E., Narti�ss, M., Pleistocene ahistory: A new insight from rounding and frosting of quartz gj.quaint.2013.08.038

The Silezers site (Fig. 2G) is located in the central part of theNorthern Vidzeme lowland. The area is characterized by a highdensity of up to 10 m high mostly parabolic dunes (Celin�s andNarti�ss, 2011). Aeolian landforms lie on top of sandy deposits ofthe Smiltene-Strenci ice-dammed/proglacial lake, formed bymelting of the Burtnieks ice lobe (Zel�cs and Markots, 2004).Currently no absolute age dates of Smiltene-Strenci lake sedimentsare available. The lake existed between the Linkuva (NorthLithuania) and Valdemarpils (Pandivere) deglaciation phases(14.5e13.8 ka, Kalm et al., 2011). A single OSL date from the top ofthe sampled Silezers parabolic dune has yielded an age of11.8 � 2.4 ka (Narti�ss et al., 2009).

2.4. North-Eastern Estonia

Two Iisaku sites (Fig. 2H,I) are located in northeastern Estonia.Aeolian deposits from these sites form parabolic dunes with arelative height up to 9.5 m and lie directly on the glaciolacustrinesediments of Glacial Lake Peipsi, correlated with the Pandiveremarginal zone of the Late Weichselian ice sheet (Hang, 2003; Kalmet al., 2011). The formation of dunes in the area started after sourcedeposits became available for aeolian redistribution (Raukas, 1999).The TL and OSL dates obtained from three vertical profiles of theIisaku dunes (Raukas and Hütt, 1988; Raukas, 1999, 2011) point tothe Holocene age of deposits e Atlantic Climatic Optimum andSubboreal time. Dune sands from two profiles east of Iisaku yieldedfive consistent dates: 4.0 ka (at 0.4 m depth), 5.9 ka (2.5 m); 4.7 ka(2.4 m), 5.4 (3.7 m) and 7.1 ka (4.8 m). Dune sands west of Iisakugave two dates: 5.2 ka (depth 0.6 m) and 6.9 ka (depth 3.5 m)(Raukas, 1999).

2.5. Western Finland

The Kalajoki site (Fig. 2J) is located in western Finland, near theGulf of Bothnia, about 40 km NE of the town of Kokkola. Theisostatic uplift of the area is causing the emergence of the seabed,

nd Holocene aeolian sediments of different location and geologicalrains, Quaternary International (2013), http://dx.doi.org/10.1016/

Fig. 2. Geological setting of aeolian sediments: A e Corralejo (Fuerteventura); B e Jaktorów N (Central Poland); C e Ko1aczek (Central Poland); D e Plecewice (Central Poland); E e

Miedzyborów (Central Poland); F e Majaks (E Latvia); G e Silezers (E Latvia); H e Iisaku 1 (NE Estonia); I e Iisaku 2 (NE Estonia); J e Kalajoki (W Finland). Lithofacies code symbolswere used according to Miall (1977, 1978).

E. Kali�nska, M. Narti�ss / Quaternary International xxx (2013) 1e12 3

Please cite this article in press as: Kali�nska, E., Narti�ss, M., Pleistocene and Holocene aeolian sediments of different location and geologicalhistory: A new insight from rounding and frosting of quartz grains, Quaternary International (2013), http://dx.doi.org/10.1016/j.quaint.2013.08.038

Fig. 3. Methodology steps (RM refers to well-rounded frosted grains; EM/RM e

partially rounded frosted grains; NU/M e non-abraded frosted grains; EL e wellrounded shiny grains; EM/EL e partially rounded shiny grains; NU/L e non-abradedshiny grains).

Fig.

4.Re

lation

ship

betw

eenAe

sum

ofroun

dedan

dsu

mof

non-

abrade

dqu

artz

grains

;Be

sum

ofae

olian-

type

andfluv

ial-type

quartz

grains

;Ce

“insitu”wea

thered

and“fresh

”grains

.


allowing sand and gravel from shallowly submerged glacial driftdeposits to be carried shoreward on the beaches (Bird, 2008). Thesubstratum sediment for dunes is glaciofluvial esker formation,which partially lies under the water of the Baltic Sea (Atlas ofFinland, 1990; Hellemaa, 1998). The first phase of dune formationin the area started 8000 cal. BP (Eronen and Olander, 1990). Theheight of the bases of the coastal dunes and the rate of the upliftindicate that the younger phase of the coastal dunes formationbegan only about 1000 cal. BP (Aartolahti, 1990), and most of thesedunes were formed during the last 500 years (Aartolahti, 1980). Thefelling of dune forests and the grazing of domestic livestock onsandy sea-shore meadows have led to the formation of present-dayactive dunes (Hellemaa, 1998).

3. Material and methods

A total of 159 samples were collected from the aeolian sedi-ments of five investigated locations. Additionally a single samplewas collected from each of the selected substratum environments:shore platform, morainic plain, sandy glaciolacustrine and aeolian.Miall’s (1977, 1978) code symbols were used to identify the lith-ofacies distinguished in some profiles (cf. Fig. 2C,FeH). The sandfraction (0.5e0.8mm) for further analysis was separated by sieving.Rounding of quartz grains (120e150 grains randomly selected fromeach sample) and frosting of their surfaces were determined underbinocular microscope with 50� magnification. The classification ofgrain shape by the Cailleux (1942) methodology, modified afterMycielska-Dowgia11o and Woronko (1998), was extended by theclassification of Krumbein (1941). Using that methodology, six

Please cite this article in press as: Kali�nska, E., Narti�ss, M., Pleistocene and Holocene aeolian sediments of different location and geologicalhistory: A new insight from rounding and frosting of quartz grains, Quaternary International (2013), http://dx.doi.org/10.1016/j.quaint.2013.08.038

0

1

2

0 1 2

Fuerteventura

Poland

Latvia

Estonia

Finland

Location

sh

ort

lon

g

0

1

2

0 1 2

coastal (warm)

coastal (cold)

coversands

dunes

Aeolian subenvironment

fluvial +

crushed

aeolian +

weathered

0

1

2

0 1 2

shore platform

aeolian

till

glaciofluvial

sandy glaciolacustrine

varved glaciolacustrine

Substratumsh

ort

lon

g

fluvial +

crushed

aeolian +

weathered

0

1

2

0 1 2

older than LGM

younger than LGM

Holocene

recent

Age group

Fig. 5. Relationship between aeolian þ weathered/fluvial þ crushed environment and long/short transportation coefficients determined against location, aeolian subenvironment,substratum and age group factors.


groups of quartz grains were determined in the sand fraction (0.5e0.8 mm): (1) EL e well-rounded shiny (Krumbein roundness 0.7e0.9); (2) RM e well-rounded frosted (Krumbein roundness 0.7e0.9); (3) EM/EL e partially-rounded shiny (Krumbein roundness0.3e0.6); (4) EM/RM e partially-rounded frosted (Krumbeinroundness 0.3e0.6); (5) C e brokenwith at least 30% of the originalgrain surface; (6) NU e non-abraded ¼ angular (Krumbein round-ness 0.1e0.2). According to the Mycielska-Dowgia11o and Woronko(1998) modification, the last NU group refers only to “fresh” quartzgrains with sharp edges without secondary transformation e NU/Lin this study. Some samples contained non-abraded quartz grainswith matt surface and thus the Cailleux (1942) classification withmodification from Mycielska-Dowgia11o and Woronko (1998) wasextended by an extra group (NU/M). A similar group has beendescribed by Bull and Morgan (2006), called “in situ” weatheredwithout effects of transport, or “OTHER” by Woronko and Hoch(2011).

Based on the analysis, all investigated grains were divided intosix groups (Fig. 3, 1st step): (1) rounded grains (RM þ EM/

Please cite this article in press as: Kali�nska, E., Narti�ss, M., Pleistocene ahistory: A new insight from rounding and frosting of quartz grj.quaint.2013.08.038

RM þ EL þ EM/EL), (2) non-abraded grains (NU/M þ NU/L), (3)frosted grains (RM þ EM/RM), (4) shiny grains (EL þ EM/EL), (4) “insitu” weathered (NU/M), and (6)“fresh” grains (NU/L) and then therelationships between the particular group of grains were deter-mined (Fig. 3, 2nd step; Fig. 4 A,B,C).

Coefficients between rounded (RMþ EM/RMþ ELþ EM/EL) andnon-rounded (NU/M þ NU/L) grains presumed to represent “long”/intense and “short”/less intense transportation (Woronko, 2012), aswell as between aeolian-type and “in situ” weathered grains(RM þ EM/RM þ NU/M) and fluvial (“water”)etype and “fresh”grains (EL þ EM/EL þ NU/L) were calculated for each sample (Fig. 3,3rd step, Table 2). Two types of the sedimentary environments andenvironmental features: (1) fluvial þ crushed, and (2)aeolian þ weathered, as well as, two types of relative trans-portation: (1) long and (2) short were distinguished (Fig. 3, 3rdstep, Fig. 5). Clusters of rounding and frosting of the quartz grainswere determined in relation to (1) aeolian subenvironment, (2)geological setting and substratum and (3) age of sediment(Table 1A,B,C, Fig. 5).


Table 1Determination of the investigated localities in relation to: A e aeolian subenvironment; B e geological setting/substratum; C e age.

A

Locality Aeolian subenvironment

Coastline dunes Inland dunes Coversands

NNE Fuerteventura Corrajero (warm environment)Central Poland Miedzyborów Plecewice

JaktorówKo1aczek

E Latvia MajaksSilezers

NE Estonia Iisaku 1Iisaku 2

W Finland Kalajoki (cold environment)

B

Locality Geological setting/substratum

Shore platform Morainic till Glaciofluvial Aeolian Glaciolacustrine(varved clays)

Glaciolacustrine(fined sands)

NNE Fuerteventura CorrajeroCentral Poland Ko1aczek Jaktorów Miedzyborów PlecewiceE Latvia Majaks

SilezersNE Estonia Iisaku 1

Iisaku 2W Finland Kalajoki

C

Locality Age

Older than LGM (>w23)a Younger than LGM (w23e10)a Holocene (w10e1)a “Recent” (<1)a

NNE Fuerteventura Corrajero(17.0e13.9)b

Central Poland Ko1aczek Jaktorów(48e39; 28e25)b

Ko1aczek JaktorówMiedzyborów (16e14 and 12;13.3e10.4)b

E Latvia MajaksSilezers (15.5e10)b

NE Estonia Iisaku 1Iisaku 2 (7.1e4.0)b

W Finland Kalajoki (1epresent)b

a Age group boundaries used in this study (in ka).b Presumed aeolian activity periods at locality (in ka).


4. Results

4.1. Relationship between rounded and non-abraded quartz grains

The number of rounded grains (RM þ EM/RM þ EL þ EM/EL) inPolish samples varies between 79.9% (Plecewice site, depth 1.5 m;Table 2) and 99.8% (Miedzyborów site, depth 1.4 m; Table 2). Asimilar content of rounded grains is noted also at the Corralejo site(68.7e89.7%). Hence, data from both locations form group A(Fig. 4A). Samples from Latvia, Estonia and Finland constitute asparser and differential group B. Group B has a smaller subgroup B1,representing more rounded quartz grains from Estonian inlanddunes and Fuerteventura coastline dunes occasionally, and a largerand elongated subgroup B2, which reveals a diminishing content ofrounded quartz grains at the Latvian, Estonian and Finnish sites.

4.2. Relationship between aeolian- and fluvial-type quartz grains

The content of aeolian-type grains (RM þ EM/RM) varies fromover 20% (E Latvia, Majaks site Fig. 4B, Table 2) to 97.58% (CentralPoland, Ko1aczek site). The mean content of aeolian-type grains isnoted at the Corrajero, Ko1aczek Jaktorów, Miedzyborów, and Ple-cewice sites (82.7, 91.3, 93.7, 93.8 and 85.23%, respectively). Hence,clusters of data (group A) from Fuerteventura and Central Poland


occur in one groupwithin values 80 to almost 100% along the x-axis(Fig. 4B). The highly remarkable (60e70%) number of aeolian-typegrains is present in some Estonian sites (Fig. 4B; group B). Group C(Fig. 4B) reveals the smallest amount (between 20 and 50%) ofRM þ EM/RM type grains, and contains both Latvian, Finnish andpartially Estonian sites (Fig. 4B).

The number of fluvial-type quartz grains (EL þ EM/EL) is thesmallest at the Fuerteventura (0%), Estonian (0e4.3%), and partiallyPolish sites, being there represented only symbolically (Fig. 4B).Some Polish and the all Latvian sites revealed larger quantities:0.8e25.8% and 0e36.7%, respectively.

4.3. Relationship between “in situ” weathered and “fresh” quartzgrains

The relationship between “in situ”weathered grains (NU/M) and“fresh” grains (NU/L) reveals three easy distinguishable groups(Fig. 4C). Group A contains Kalajoki site (W Finland) with thehighest number (20 to almost 50%) of sharp-edged grains withoutthe secondary transformation (NU/L), and the moderately number(up to 35%) of “in situ” weathered grains (NU/M). Group B repre-sents two tendencies: (1) with the increasing number (up tow35%)of NU/L grains (Polish sites), and (2) with the increasing number(up to w18%) of NU/M grains represented by Fuerteventura site. In


Table 2Selected results of the Cailleux analysis (1942) with the modification of Mycielska-Dowgia11o and Woronko (1998) of the selected profiles/points in the investigated locations: 1 e Ʃ aeolian-type (RM þ EM/RM) grains [%], 2 e Ʃaeolian-type (RM þ EM/RM) and “in situ” weathered (NU/M) grains [%], 3 e Ʃ fluvial-type (EL þ EM/EL) grains [%], 4 e Ʃ fluvial-type (EL þ EM/EL) þ “fresh” (NU/L) grains [%], 5 e Ʃ non-abraded (NU/L þ NU/M) grains [%], 6 e Ʃrounded (RM þ EM/RM þ EL þ EM/EL) grains [%], 7 e fluvial þ “crushing” (EL þ EM/EL þ NU/L) to aeolian þ “weathering” (RM þ EM/RM þ NU/M) grains coefficient, 8 e non-abraded (NU/L þ NU/M) to rounded (RM þ EM/RM þ EL þ EM/EL) grains coefficient.

Locality Name of profile/point

Depth [m]/part ofpoint

Type of grains [%] 1 2 3 4 5 6 7 8

Aeolian-typegrains

“In situ”weatheredgrains

Fluvial-typegrains

“Fresh” grains

RM EM/RM NU/M EL EM/EL NU/L

Fuerteventura Corralejo Windward slope 1.4 88.3 10.3 0 0 0 89.7 100 0 0 10.3 89.7 0 0.11Leeward slope 18.26 71.43 7.14 0 0 0 89.69 96.83 0 0 7.14 89.69 0 0.08Crest 17.4 51.3 26.95 0 0 0 68.7 95.65 0 0 26.95 68.7 0 0.39Substratum 12.3 62.3 25.4 0 0 0 e

Central Poland Ko1aczek 0.5 5.92 83.7 0 0 6.66 0 89.62 89.62 6.66 6.66 0 96.28 0.07 00.7 0 96 0 0 2.4 0 96 96 2.4 2.4 0 98.4 0.03 00.9 1.38 93.75 0.69 0 2.77 0 95.13 95.82 2.77 2.77 0.69 97.9 0.03 0.011.4 24.19 73.39 0 0 0.81 0 97.58 97.58 0.81 0.81 0 98.39 0.01 01.45 0 81.7 0 0 16.99 0 81.7 81.7 16.99 16.99 0 98.69 0.03 0.011.6 0 98.4 0 0 0.78 0 98.4 98.4 0.78 0.78 0 99.2 0.01 01.75 0.68 89.04 0 0 8.9 0 89.72 89.72 8.9 8.9 0 98.62 0.1 01.8 1.41 88.03 0 0 8.45 0 89.44 89.44 8.45 8.45 0 97.89 0.1 02.0 0 91.55 0 0 7.04 0 91.55 91.55 7.04 7.04 0 98.59 0.1 02.2 1.36 82.19 0 0 14.38 0 83.55 83.55 14.38 14.38 0 97.93 0.17 0Substratum 2.05 76.4 3.2 0 13.2 0 e

Jaktorów 0.5 0 93.85 0 0 5.38 0 93.85 93.85 5.38 5.38 0 99.23 0.06 00.7 0.68 92.46 0 0 4.79 0 93.14 93.14 4.79 4.79 0 97.93 0.05 00.8 2.03 94.59 0 0 2.7 0 96.62 96.62 2.7 2.7 0 99.32 0.03 01.1 4.25 87.23 0 0 6.38 0 91.48 91.48 6.38 6.38 0 97.86 0.07 0

Plecewice(Kali�nska, 2012)

0.4 29.22 58.44 8.44 0 1.95 0 87.66 96.1 1.95 1.95 8.44 89.61 0.02 0.090.6 9.42 83.33 0.72 1.44 3.62 0 92.75 93.47 5.06 5.06 0.72 97.81 0.05 0.010.7 14.28 71.43 2.04 0 10.2 0 85.71 87.75 10.2 10.2 2.04 95.91 0.12 0.020.8 10.6 59.6 0.66 0.66 25.16 0 70.2 70.86 25.82 25.82 0.66 96.02 0.36 0.011.0 21.43 59.52 12.5 2.97 2.38 0 80.95 93.45 5.35 5.35 12.5 86.3 0.06 0.141.1 12.34 68.18 8.44 0.65 9.74 0 80.53 88.96 10.39 10.39 8.44 90.91 0.12 0.091.2 21.8 71.43 5.26 0 0.75 0 93.23 98.49 0.75 0.75 5.26 93.98 0.01 0.061.3 21.8 71.43 3 3 0 0 93.23 96.23 3 3 3 96.23 0.03 0.031.4 9.03 83.33 2.77 0 4.86 0 92.36 95.13 4.86 4.86 2.77 97.22 0.05 0.031.5 12.57 66.04 15.72 0 1.25 0 78.61 94.33 1.25 1.25 15.72 79.86 0.01 0.21.6 17.86 75 3.57 0.71 2.15 0 92.86 96.43 2.86 2.86 3.57 95.72 0.03 0.041.7 23.33 60 7.33 0 6.66 0 83.33 90.66 6.66 6.66 7.33 89.99 0.07 0.081.8 12.9 72.58 12.09 0 1.61 0 85.48 97.57 1.61 1.61 12.09 87.09 0.02 0.141.9 15.92 60.51 6.37 2.55 7.0 0 76.43 82.8 9.55 9.55 6.37 85.98 0.11 0.07

Miedzyborów 0.8 93.0 0 0 0 6.0 0 93.0 93.0 6.0 6.0 0 99.0 0.06 01.4 97.0 0 0 0 2.8 0 97.0 97.0 2.8 2.8 0 99.8 0.03 02.2 89.0 2.0 0 0 8.1 0 89.0 91 8.1 8.1 0 99.1 0.09 03.0 94.0 0 0 0 5.2 0 94.0 94.0 5.2 5.2 0 99.2 0.06 03.5 95.5 0 0 0 4.1 0 95.5 95.5 4.1 4.1 0 99.6 0.04 04.0 94.4 0 0 0 2.8 0 94.4 94.4 2.8 2.8 0 97.2 0.03 0Substratum 86.2 0.8 0 0 11.1 0 e

Latvia Silezers 2.0 8 23.2 64 0.8 3.2 0 31.2 95.2 4.0 4.0 64 35.2 0.04 1.822.8 13.38 35.43 37.8 0 5.51 0 48.81 88.61 5.51 5.51 37.8 54.32 0.06 0.693.1 8.45 27.46 59.86 0 3.53 0 35.91 95.77 3.52 3.52 59.86 39.53 0.04 1.523.3 9.09 29.37 53.85 0 0.69 0 38.46 92.31 0.69 0.69 53.85 39.15 0.01 1.373.5 10.4 42.4 33.6 0 6.4 0 52.8 86.4 6.4 6.4 33.6 59.2 0.07 0.573.7 8.22 29.11 54.43 0.63 1.89 0 37.33 91.76 2.52 2.53 54.43 39.85 0.03 1.364.0 1.94 32.36 59.35 0 1.93 0 34.3 93.55 1.93 1.93 59.35 36.13 0.02 1.64

(continued on next page)

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Table 2 (continued )

Locality Name of profile/point

Depth [m]/part ofpoint

Type of grains [%] 1 2 3 4 5 6 7 8

Aeolian-typegrains

“In situ”weatheredgrains

Fluvial-typegrains

“Fresh” grains

RM EM/RM NU/M EL EM/EL NU/L

4.1 11.93 16.51 32.11 0 4.58 32.11 28.44 60.55 4.58 36.69 64.22 33.02 0.61 1.944.3 8.33 22.73 56.82 0 2.7 0 31.06 87.88 2.7 2.27 56.82 33.33 0.03 1.74.5 4.94 32.1 59.26 0 1.23 0 37.04 96.3 1.23 1.23 59.26 38.27 0.01 1.554.6 6.66 32 53.3 0.66 2 0 38.66 91.96 2.66 2.66 53.3 41.32 0.03 1.294.8 5.14 42.65 35.29 0 10.29 0 47.79 83.08 10.29 10.29 35.29 58.08 0.12 0.615.0 7.14 36.43 50.0 0 2.14 0 43.57 93.57 2.14 2.14 50.0 45.71 0.02 1.09Substratum 6.98 33.33 51.94 1.55 3.88 0 40.31 92.25 5.43 5.43 51.94 45.74 0.10 1.13

Majaks 0.7 5.84 40.15 43.1 0.73 8.75 0 45.99 89.09 9.48 9.48 43.1 55.47 0.11 0.781.1 9.09 28.92 52.06 0 2.48 0 38.01 90.07 2.48 2.48 52.06 40.49 0.03 1.291.3 5.15 42.64 40.44 0.73 4.41 0 47.77 88.23 5.14 5.14 40.44 52.93 0.06 0.761.35 10.07 25.17 43.16 0 6.47 0 35.24 78.4 6.47 6.47 43.16 41.71 0.08 1.031.5 3.33 25.0 50.83 0 10.0 0 28.33 79.16 10.0 10 50.83 38.33 1.13 1.331.9 7.97 25.36 56.52 0.72 5.79 0 33.33 89.85 6.51 6.51 56.52 39.84 0.07 1.422.1 8.0 32.0 35.2 1.6 19.2 0 40.0 75.2 20.8 20.8 35.2 60.8 0.28 0.582.5 5.0 20.0 52.14 0 16.43 0 25.0 77.14 16.43 16.43 52.14 41.43 0.21 1.262.6 10.53 29.82 47.37 0 9.65 0 40.35 87.72 9.65 9.65 47.37 50 0.11 0.952.8 11.29 25.0 49.19 0 10.43 0 36.29 85.48 10.43 10.43 49.19 46.72 0.12 1.052.9 13.71 26.61 45.96 0.8 10.48 0 40.32 86.28 11.28 11.28 45.96 51.6 0.13 0.893.0 11.94 20.15 54.47 0 9.7 0 32.09 86.56 9.7 9.7 54.47 41.79 0.11 1.33.2 8.66 14.7 59.05 0.78 12.59 0 23.36 81.88 13.37 13.37 59.05 36.2 0.16 1.633.5 10.57 29.26 46.34 0.81 11.38 0 39.83 86.17 12.11 12.19 46.34 52.02 0.14 1.023.7 14.28 36.84 30.83 0.75 9.02 0 51.12 81.95 9.77 9.77 30.83 60.89 0.12 0.51

Estonia Iisaku 1 0.5 15.2 54.4 27.2 0 0.8 0 69.6 96.8 0.8 0.8 27.2 70.4 0.01 0.390.7 18.93 43.18 34.82 0 0 0 62.11 96.95 0 0 34.84 62.11 0 0.561.1 10.32 41.27 45.25 0 3.17 0 51.59 96.83 3.17 3.17 45.24 54.76 0.03 0.831.5 17.24 35.34 45.68 0 0.86 0 52.58 98.26 0.86 0.86 45.68 53.44 0.01 0.851.8 11.51 41.0 41.0 0 2.16 0 52.51 93.51 2.16 2.16 41 54.67 0.02 0.752.5 24.6 39.68 30.95 0 3.96 0 64.28 95.23 3.96 3.96 30.95 68.24 0.04 0.452.7 28.57 25.0 38.57 0 4.28 0 53.57 92.14 4.28 4.28 38.57 57.85 0.05 0.673.1 19.38 31.0 42.63 0.77 3.1 0 50.38 93.01 3.87 3.87 42.63 54.25 0.04 0.78

Iisaku 2 1.5 13.53 25.56 57.89 0 0 0 39.09 96.98 0 0 57.89 39.09 0 1.482.1 23.07 36.15 36.15 0 3.84 0 59.22 95.37 3.84 3.84 36.15 63.06 0.04 0.572.3 12.39 41.32 42.97 0 1.71 0 53.71 96.68 1.71 1.71 42.97 55.42 0.02 0.772.4 8.69 28.26 30.71 0 2.36 0 36.95 67.66 2.36 2.36 30.71 39.31 0.03 0.782.5 12.97 25.95 54.96 0 3.82 0 38.92 93.88 3.82 3.82 54.96 42.74 0.04 1.292.7 12.87 27.27 53.03 0 3.78 0 40.14 93.17 3.78 3.78 53.03 43.92 0.04 1.212.8 17.54 28.94 42.11 0 2.63 0 46.48 88.59 2.63 2.63 42.11 49.11 0.03 0.883.0 16.92 35.38 41.53 0.77 0.77 0 52.3 93.83 1.54 1.54 41.53 53.84 0.02 0.773.1 10.63 32.62 48.23 0 4.25 0 43.25 91.48 4.25 4.25 48.23 47.5 0.05 1.02

Finland Kalajoki Foredune 24.06 21.8 21.8 0.75 0.75 22.56 45.86 67.66 1.5 24.06 44.36 47.36 0.35 0.94Yellow dune 13.51 31.76 16.22 0 0 25.58 45.27 61.49 0 25.58 41.8 45.27 0.42 0.92Transitional zone 14.17 26.67 29.17 0 0 26.67 40.84 70.01 0 26.67 55.84 40.84 0.38 1.37Backdune 17.46 28.57 20.63 1.59 2.38 26.19 46.03 66.66 3.97 30.16 46.82 50.0 0.45 0.94

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contrast, group C, containing both Estonian and Latvian localities,spreads along the x-axis with “in situ” weathered grains consti-tuting 20 to over 60%.

4.4. Relationship between environmental conditions/transportationcoefficient- location factor

The quartz grains of all investigated sites reveal an aeolian/“in-situ” weathered environment (Fig. 5 e Location) with a slightlysmaller (i.e. Finnish or some Latvian and Polish sites) or higher (i.e.Polish, Fuerteventura, Latvian and Estonian sites) content of aeolian“in situ” grains. The cluster of data from Estonian and Latviansamples is spread along the y-axis and reflects a highly variableduration of sediment transportation (short/long). Long-term,aeolian sedimentary conditions are mostly represented at thePolish and Fuerteventura sites. Finnish and partially Latvian dataare widespread with the greatest admixture of both aeolian- andfluvial-type quartz grains (but with the prevalence of aeolian-type),controlled by short- as well as long-term transportation.

4.5. Relationship between environmental conditions/transportationcoefficient e aeolian subenvironment factor

Three types of aeolian subenvironments were distinguished(Fig. 5 e Aeolian subenvironment): (1) coastal dunes, (2) inlanddunes and (3) coversands (sand sheets), which have no slip faces(McKee, 1979; Kocurek and Nielson, 1986). Based on the longitu-dinal characterization, the group of coastal dunes was subdividedinto two subgroups, those formed in: (i) warm conditions (Fuer-teventura) and (ii) cold conditions (W Finland). The cluster ofdata (Fig. 5 e Aeolian subenvironment) representing thedune subenvironment spreads along the y-axis and reveals both awide transportation variability and deposition in theaeolian þ weathering sedimentary environment. Quartz grainsderived from the coversands occupy the “0e0” corner of thescheme, pointing to a subenvironment with the longest/highestdegree of transportation and aeolian properties. Seemingly, thegroup of coastal dunes is located in the opposite parts of thescheme, showing: (i) a mixture of aeolian (majority) and fluvial(minority) types of relatively short-transported grains (“cold”coastal dunes) and (ii) relatively well-rounded grains representingtypical aeolian conditions (“warm” coastal dunes).

4.6. Relationship between environmental conditions/transportationcoefficient e substratum sediments factor

Three distinct groups were differentiated based on the geolog-ical setting and substratum conditions (Fig. 5 e Substratum): (1)four types of data located in the “0e0” corner with the relativelystrongest aeolian and the relatively longest transportation charac-teristics: (i) with a shore platform, (ii) morainic, (iii) aeolian and (iv)glaciolacustrine with the varved clay substratum; (2) a cluster withsandy glaciolacustrine sediment substratum extending along the y-axis in the relatively most intensive highest aeolian þ weatheredconditions, but changeable transportation, and (3) a widely spreadcluster of data with glaciofluvial substratum.

4.7. Relationship between environmental conditions/transportationcoefficient e age factor

Four relative age groups (Table 1C) (1) older than the Last GlacialMaximum (LGM), (2) younger than the LGM, (3) Holocene and (4)“recent” (younger than 1000 cal. BP (Aartolahti, 1990)) wereintroduced to find a relationship between the age of the investi-gated sediments and their textural development (Fig. 5 e Age


group). The group of the oldest (“older than LGM”) sediments oc-cupies part of the x-axis and suggests the greatest roundness ofgrains and relatively highest degree of matting. On the whole, thecluster representing the “younger than LGM” age spreads along they-axis and indicates aeolian þ weathered treatment with a differ-ential duration of the transporting. The “Holocene” cluster gener-ally coincides with the “younger than LGM” group, but differs bythe lack of grains representing the longest transportation. The“recent” cluster spreads within both the longer and shorter trans-portation, reaching the border between aeolian and fluvial accu-mulative environments.

5. Discussion

An analysis of surface texture and roundness of quartz sandgrains from sediments of different locations, geological settings andaeolian subenvironments revealed a predominance of mattedgrains in all five investigated locations. It suggests subaerial envi-ronments with the predominance of the aeolian factor (Cailleux,1952; Krinsley and Doornkamp, 1973; Pye, 1984; Mycielska-Dowgia11o and Woronko, 2004; Velichko et al., 2011), both in cold(Central Poland, E Latvia, NE Estonia and W Finland) and warm(Fuerteventura) climatic conditions. Along with the grain round-ness and surface features common to all considered areas, somedifferences were recorded. In the most northern locality (WFinland), shiny and non-abraded grains are found together withdifferent types of grains of aeolian and “in situ” weathered origin.Such a combination may be caused by (1) the influence of glacio-fluvial/beach substratum and/or (2) short-term accumulation andtransforming processes. The Finnish Kalajoki site reflects the in-termediate or low “maturity” of aeolian quartz grains, which isconsistent with aeolian sediment features observed in Lapland(Seppälä, 1969, 1971) and Central Sweden (Mycielska-Dowgia11o,1993). Such properties could be expected, because in cold envi-ronments mineral material is often a very fresh weathering productof crystalline rocks, or ground by the glacier, and after that trans-ported by water over only short distances before aeolian drifting(Seppälä, 2004).

The diversity of quartz grains at the most northern sites (WFinland, NE Estonia) could be explained by only brief activity ofaeolian processes during the decline of the Late Weichselian icesheet. The “recent” age cluster reveals a high variability in theroundness and frosting of quartz grains, while the “Holocene” oneis characterized by a larger number of aeolian-type grains, but aschangeable in their shape as the “recent” group. At the same time,the Polish sites, yielding the oldest age (older and younger than theLGM), are located in the opposite corner of the scheme with thehighest rounding and frosting of grains. A similar pattern can beobservedwhen comparing rounding and frosting of quartz grains ofthe modern dune deposits in both Central Poland, Southern Swe-den and Belgium (Mycielska-Dowgia11o,1989,1993), andwithin themeridional profile from Central (beyond the extent of the Weich-selian ice sheet) to Northern Poland (within the extent of theWeichselian glaciation) (Go�zdzik, 1991, 1995).

The distribution of the “younger than LGM” sample cluster(Latvian and Fuerteventura locations) along the y-axis shows hugedifferences in the roundness of quartz grains. Such a combination ofgrains precludes the aforementioned pattern introduced for Polandand Sweden by Mycielska-Dowgia11o (1989, 1993) and Go�zdzik(1991, 1995). Considering that all data of the group are correlatedwith approximately the same time and that the aeolian processesresponsible for dune formation lasted for several thousand yearsduring the decline of the last glaciation, the highest degree ofroundness could (1) be inherited from the substratum sedimentsor/and (2) reflect the geological/environmental history of the



particular regions, and/or (3) record the unique conditions/eventsduring/after accumulation of sediments. Judging both from thesubstratum of sediments and their age, it is clear that the aeoliansand of the Fuerteventura site was derived from a marine sourceand sea-level changes affected the mobility of dunes in that area(Hesp and Thom, 1990). Similar compatibility has been noticed alsoin different parts of the world (Sheperd, 1985; Clement et al., 2010).In contrast, the Quaternary aeolian deposits in the northeasterncoastal part of Tunisia revealed (Chakroun et al., 2009) a low per-centage of rounded grains. The Latvian group of aeolian sands,which belongs to the same age cluster as Fuerteventura (trans-formation time of aeolian sediments was approximately the same),is enriched in the mixture of non-abraded quartz grains and revealsfeatures of poor/short transporting. Domination of parabolic dunesand presence of blow-outs at the Latvian sites (Celin�s and Narti�ss,2011) has usually been connected with partial stabilization byvegetation and/or moisture (McKee, 1979). Thus both the texturalfeatures and morphology of dunes at the Latvian sites suggest poorconditions for aeolian reworking of sand.

The investigations in the southeastern part of the “EuropeanSand Belt” in the Western Ukraine (Zieli�nski et al., 2009) yielded arelatively high content of well- and partially-rounded quartz grainsin the aeolian sediments. Compared to analogous sediments fromthe Polish Lowland, the content of aeolian-type grains at the pre-viously mentioned site is slightly smaller to the advantage of shiny(water-type grains). The advantage of shiny-type grains wasexplained by the local palaeoenvironmental conditions includingthe presence of steppe and forest steppe areas (Büdel, 1948;Gerasimov and Velichko, 1982), which as a vegetation may haveslightly impeded the intensity of aeolian processes (Zieli�nski et al.,2009). Observations of textural features in theWestern Ukraine andE Latvia thus do not confirm the meridional hypothesis ofMycielska-Dowgia11o (1989, 1993) and Go�zdzik (1991, 1995).

The quartz grains extracted from the Finnish Kalajoki site aremore similar to glaciofluvial than aeolian deposits, and representmixtures of all types of grains. Usually coarse-grained glaciofluvialdeposits (Gibbard and Lewin, 2002) are extremely heterogeneousin the types of micromorphology of quartz sand grain surfaces,which were shaped in many environments (Mycielska-Dowgia11oand Woronko, 2004). These grains were incorporated in the icemass and subsequently released into glaciofluvial stream andaccumulated as sub-aqueous deposits. Hence, a large number ofangular (NU) and cracked (C) grains is noted in glaciofluvial sedi-ments (Woronko, 2001). In contrast, the aeolian sediments groupedin the typical aeolian conditions and the long transportation corner(Fig. 5 e Substratum) reveal a high variety of quartz grain types intheir substratum (aeolian and glaciolacustrine sediments, morainictill and shore platform sediments). Such a combination may beattributed to enrichment of some deposits, i.e. lacustrine or alluvialin aeolian-type grains during the climatic conditions controlled byaeolian activity over vast areas (Lewkowicz and Young, 1991;Vanderberghe and Ming-koo, 2002; Mycielska-Dowgia11o andWoronko, 2004). An increase in aeolian-type quartz grains (RM andEM/RM) is also noted in tills (Woronko, 2001) as a process of glacialabrasion of the substratum in time and space (Mycielska-Dowgia11oandWoronko, 2004). Hence, many quartz grains could be reworkedfrom glacial environments and mixed with aeolian deposits(Mahanay and Andres, 1991; Mahanay, 1992a,b).

Recent observations of very well-sorted sandwithwell-roundedand frosted grains among widespread aeolian deposits in VictoriaValley, Antarctica (Hambrey and Fitzsimons, 2010), which arederived from fluvial sediments by katabatic wind action (Lancaster,2002), are in high contrast to observed properties of late glacial/early Holocene dunes of Latvia. Thus, observations of aeolian sed-iments from cold environments (Finland, Estonia, Latvia and


Antarctica) suggest a high influence of substratum (source mate-rial) properties on aeolian sediments due to poor reworking ofmaterial. This observation is confirmed also by presence of therelatively high amount of well-rounded (RM) grains (up to 24.06%,28.57 and 14.28% in Finland, Estonia and Latvia, respectively),presumably incorporated into aeolian transportation from glacio-fluvial/beach (Finland) and glaciolacustrine (Estonia and Latvia)settings. The latter setting contains grains inherited from under-lying Devonian sandstones, as a relatively high content of well-rounded Devonian quartz grains has been observed in local tillsand glaciofluvial sediments of the last glaciation (Mahaney et al.,2000).

Comparison of the types of quartz grains with aeolian sub-environments shows that all investigated subenvironments con-taining both up to a few metres-high dunes and shapelesscoversands can be built by grains representing different degrees ofaeolian transport. Both the flat coversands and the dunes yield thehighest degree of aeolian transformation. Moreover, the texturalfeatures of coversands from Central Poland are comparable withdune deposits from the same area (Kali�nska, 2012). In contrast toLatvian and Estonian sites, up to 10-m high dunes contain a largevariety of aeolian-type grain shapes. A similar relation has beenobserved in Sweden, where short total duration of aeolian pro-cesses after deglaciation and before expansion of vegetationresulted in distinct dune forms (Seppälä, 1972).

Grains of the sediments of the most contrasting climatic local-ities, Fuerteventura and Finland, but theoretically of the samecoastline sedimentary environment, reveal both the lowest and thehighest degree of grain transformation (Finland and Fuerteventura,respectively). The surface of quartz grains from cold environmentscould reflect the effect of both aeolian and sub-aqueous trans-portation as an inheritance of glacial, sub-aqueous and aeolianfeatures (Kotilainen, 2004). In contrast to the Fuerteventura site,grains of aeolian sediments from lower latitudes could also behaveas poorly transformed clasts (Wasson, 1983; McTainsh, 1989;Nanson et al., 1995; Newsome, 2000; Fitzsimmons et al., 2009).Those different patterns of grain shape and surface imply regionalsetting and individual signature of sediments.

6. Conclusions

All investigated localities revealed the prevalence of aeolian-type grains, which points to the predominance of the aeolian fac-tor in their transformation. The rounding and frosting analysisexhibited a great variability within quartz grains of the sand frac-tion (0.5e0.8 mm), hence certain differences in the sediments weredistinguished.

The relationship between the age of sediments and the degreeof aeolian transformation of quartz grains holds true for only in thecase of the youngest (the Finnish one) and the oldest (the Polishone) clusters of sediments. The youngest cluster yielded thesmallest transformation and a mixture of grains of different origin,while grains of the oldest cluster are the most aeolian-type andhomogeneous in shape.

The meridional impact of aeolian processes connected with thedecline of the Last Glacial Maximum (LGM) was observed in boththe “recent”, Holocene age group of samples and the older thenLGM cluster. The “recent” group, as the youngest one, represents ahigh variability of quartz grains both in shape and the surface type.The Holocene group, which developed a few thousand years longer,reflects the same variability range of grain shape, but with traces ofaeolian activity on their surface. The oldest cluster of data (olderthan LGM ¼ part of the Polish sites) revealed the highest trans-formation of quartz grains, comprising homogeneous, well-rounded and frosted quartz grains.



The “younger than LGM” cluster provided awide range of quartzgrain types from well-rounded to non-abraded grains. Three rea-sons for such a high variability include: (1) inheritance after thesubstratum sediments, (2) geological history of the particular re-gion/setting and (3) unique environmental conditions during/afterthe accumulation of the sediment.

The most northern (Finnish Kalajoki) site reflects distinct fea-tures typical of that latitude e variability in both rounding andfrosting of quartz grains of the sandy (0.5e0.8 mm) fraction. In-heritance of some elements after the adjacent sedimentary envi-ronments and short-term transformation of quartz grains have beennoted. Cold-environment aeolian sediments are weaker reworkedand have better preserved pre-aeolian sand textural properties.

No relationship between the transformation degree of grainsand advancement of aeolian subenvironment was detected. Bothwell-developed dunes and shapeless coversands could revealprevalence of well-rounded (RM) and partially rounded matt (EM/RM) quartz grains, whereas up to few metres high dunes could bebuilt of themixture of different types of grains derived fromvarioussedimentary environments.

No relationship between textural features of quartz grainslocated in the same aeolian subenvironment (coastline dunes), butin two contrasting climatic environments (cold and warm) wasdetermined. Only the regional geological setting could imply thesignature of quartz grains.

Acknowledgments

The authors express their thanks to Katrin Lasberg (University ofTartu), Alexander Gorlach (University of Tartu) and Ivars Celin�s(University of Latvia) for help in the fieldwork. The referees forhelpful comments on the manuscript. The study was partiallyfunded by the Postdoctoral Research Grant ERMOS (FP7Marie CurieCofund the “People” programme) “Age and climatic signature ofcoversands deposits distributed on glaciolacustrine basins alongthe Scandinavian Ice Sheet margin southeast of the Baltic Sea”.

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