Studia Quaternaria, vol. 31, no. 1 (2014): 51–60. DOI: 10.2478/squa-2014-0005

LATE HO LO CENE CHANGES IN VEG E TA TION OF THE MR¥GOWOLAKELAND (NE PO LAND) AS REG IS TERED IN THE POL LEN

RE CORD FROM LAKE SALÊT

Marta Szal1, Mi ros³awa Ku pry janowicz1, Mari usz Wyczó³kowski2

1 In sti tute of Bi ol ogy, Uni ver sity of Bia³ystok, Œwierkowa 20b, 15-950 Bia³ystok, Po land; e-mail: martaszal@op.pl, m.kupryjanowicz@uwb.edu.pl2 Wojciech Kêtrzyñski Mu seum, Plac Zamkowy 1, 11-400 Kêtrzyn, Po land; e-mail: mw@muzeum.ketrzyn.pl

Ab stractPol len anal y sis of sed i ments from the up per part of bot tom de pos its from Lake Salêt al lowed re con struc tion of mainstages of the Late Ho lo cene veg e ta tion trans for ma tion in the Mr¹gowo Lake Dis trict (from ca. 3600 cal. years BC) and to cor re late some of these changes with im mi gra tion and eco nomic ac tiv ity of lo cal hu man groups. Sig nif i cant spread -ing of sec ond ary semi-nat u ral birch for est, de vel op ment of horn beam for est and in creas ing im por tance of anthro-pogenic open com mu ni ties were the most char ac ter is tic fea tures of veg e ta tion evo lu tion. A def i nite break down of elmtook place be tween 2900 and 2500 cal. years BC, slightly af ter in creased con tri bu tion of birch in wood lands. Dis ap -pear ance of ha zel around 1200 cal. years BC, ac com pa nied by ex pan sion of horn beam has been ob served and shouldbe linked with ac tiv ity of the Z¹bie-Szestno type cul ture and the Lusatian cul ture tribes dur ing the Bronze Age, but not with a cli mate change. Con sid er able in ten si fi ca tion of set tle ment pro cesses re corded in the youn ger part of the Subat-lantic chronozone was one of the im por tant rea sons that were re spon si ble for quick changes in for est struc ture. Strongand con tin ued de for es ta tion started as early as the end of the 10th cen tury AD and was sub stan tially in ten si fied in thefirst half of the 13th cen tury.

Key words: veg e ta tion trans for ma tions, Late Ho lo cene, pol len anal y sis, Mr¹gowo Lake Dis trict, Masuria, NE Po land.

Manu script re ceived 28 October 2013, ac cepted 14 May 2014

IN TRO DUC TION

Pol len anal y sis is one of the most widely used re searchtools in paleoecology that helps in de tect ing re sponses of nat -u ral veg e ta tion to hu man im pacts through his tory, as well asto cli mate and en vi ron men tal change on a va ri ety of tem po ral and spa tial scales (e.g. Prentice, 1988; Hunt ley, 1990). Pol -len re cords have been used to study biostratigraphy, veg e ta -tion pat terns and agrar ian his tory of the Masurian Lakelandfor many years. Among the sites that have been paly no logi -cal ly ex am ined within mod ern stan dards, only a few in -cluded pol len se quences cov er ing the Subatlantic chrono-zone. These were pol len se quences from: Lake Miko³ajskie(Ralska-Jasiewiczowa, 1966), Lakes Kruklin, Mamry andTa³ty (Stasiak, 1967, 1971), Lake Dga³ Wielki (Filbrandt-Czaja, 2000), Lakes Mi³kowskie, Wojnowo and £azduny,for mer Lake Staœwiñskie and the Szczepanki site (Wacnik,2009a, b; Wacnik et al., 2012a), Wielkie B³oto mire (Kar-piñska-Ko³aczek et al., 2013) and Skaliski For est (Ko³aczeket al., 2013). How ever, be yond the pro files de scribed byWacnik (2009a, b; Wacnik et al., 2012a) most stud ied se -quences were poorly sup ported by ra dio car bon dat ing, or theages were miss ing. This fact re stricted pos si ble re con struc -tion of rate of en vi ron men tal changes and their cor re la tionwith ar chae o log i cal, his tor i cal and cli ma tic data.

From a paleoecological per spec tive north east ern Po landis an in ter est ing re gion, be cause it is un der in flu ence of atran si tional cli mate (e.g. Woœ 1999). Oc cur rences of dif fer -ent air masses have wide range of in flu ence upon nat u ral dis -tri bu tions of plants typ i cal for both the mar i time (e.g. Cla-dium mariscus and Juncus subnodulosus) and the bo real cli -mate (among oth ers: Polemonium caeruleum, Nymphaeacandida and Nuphar pumila; Ga³ka et al., 2014). Such spe -cific char ac ter of this part of Po land is re flected also in geo-bo tan i cal di vi sion of the coun try, in which it was in cluded inthe Masuria-Belarus North Di vide (Matuszkiewicz 2008).Palaeo eco logi cal re search in this area is a key to un der stand -ing of mech a nisms and rea sons for plant mi gra tion (Kupryja- nowicz 2008; Lamentowicz et al., 2008). To as sess, to whatex tent the re cords from mar i time and more con ti nen tal re -gions are dif fer ent from one an other, more re search and es pe -cially multi-proxy in ves ti ga tion is needed.

Ar chae ol o gists have al ready dem on strated a spe cific and unique char ac ter of eco nomic ac tiv ity in north east ern Po landin re la tion to cen tral Eu rope (e.g. Okulicz 1973; Karczewski2011). A par tic u lar fea ture of this area was a pro longed ex is -tence of for ag ing and a very late ac cep tance of farm ing as theba sis for food pro cure ment, in con trary to the rest of Po land(Wacnik et al., 2012a).

This study is fo cused on re con struc tion of the Late Ho lo -cene veg e ta tion changes in the Mr¹gowo Lake Dis trict,based on pol len anal y sis and sup ported by AMS ra dio car bondat ing. The pri mary aim was to pres ent veg e ta tion de vel op -ment in the sur round ings of Lake Salêt from ca. 3600 cal.years BC and to pro vide data for eval u a tion of wood landtrans for ma tion by a man.

MA TE RIAL AND METH ODS

De scrip tion of the study site

Lake Salêt (53°56'22.09"N, 21°19'20.19"E) is a eutro-phic wa ter body with area of 327.7 hect ares (Jañczak, 1999).It is lo cated be tween the vil lages Szestno, Ruska Wieœ,Brodzikowo and Wyszembork in the cen tre of the Mr¹gowoLake Dis trict, which is a part of the Masurian Lake Dis trict innorth east ern Po land (Fig. 1).

The lake is of gla cial or i gin and is lo cated in a de pres sionsur rounded by morainic hills. Steep es carp ments, over 10 mhigh, slope down to the wa ter sur face on both east ern andwest ern lakesides; whereas north ern and south ern slopes aremore gen tle. The lake is di vided into two parts – the smaller,north ern part is named Lake Salêt Ma³y and the larger south -ern part is Lake Salêt Wielki (Fig. 1). Max i mum wa ter depthis 17.2 m and mean depth is 4.9 m (Jañczak, 1999). The lakeis fed by a sin gle stream and in ad di tion to sur face run off, aninflow of shal low un der ground wa ter from the sur round ingmo raine up land is prob a bly also pos si ble.

The veg e ta tion around Lake Salêt is al most de void offor est and in di cates sub stan tial anthropogenic changes. Thefor est oc curs in 10% of the area only whereas most is oc cu -pied by grass lands: mead ows and pas tures 30%, ar a ble landof 60%. A land strip of 500 m around the lake is over grownby her ba ceous veg e ta tion, with scat tered trees oc cur ring near build ings, along roads and streams and at the lakeshore only.

Cor ing and dat ing

In win ter 2010 a core of sed i ments was taken from thefrozen sur face of Lake Salêt with the use of the Wiêc-kowski’s pis ton corer and the Kajak grav ity corer. Cor ingwas per formed close to the deep est part of the lake (wa terdepth 15 m), with bot tom de pos its 15.70 m thick (Fig. 1). The pres ent pa per deals with a top part of the log only (depth to10.80 m). This part of the core is com posed of cal car e ousgyttja, rich in or ganic mat ter and rel a tively poor in sand, clayand silt.

AMS ra dio car bon dat ing of seven pol len con cen tratesam ples was per formed in the Gliwice Ab so lute Dat ingMeth ods Cen tre (Ta ble 1). The iso la tion of pol len con cen -trates from the sed i ment was per formed by re moval of cal -cium car bon ate us ing 38% HCl and humic ac ids, us ing 10%KOH and 2–4 cm2 of sed i ment was used for this pur pose.

Short-lived radionuclides 210Pb were mea sured in the up -per most layer, 30 cm thick. The anal y sis was car ried out inthe In sti tute of Geo log i cal Sci ences of the Pol ish Acad emy of Sci ences in War saw.

52 M. SZAL et al.

Fig. 1. Lo ca tion of Lake Salêt and cor ing site.

Ta ble 1AMS ra dio car bon dat ing of sed i ments from Lake Salêt

No. Depth (cm) Lab. No. Age 14C (BP) Cal i brated age range 95% (BP) Cal en dar age

1 330 GdA-2979 830±25 785 (95.4%) 689 1116-1261 A.D.

2 370 GdA-2980 1090±251058 (92.6%) 953947 ( 2.8%) 939

892-1011 A.D.

3 410 GdA-2981 1275±251284 (94.6%) 11711155 ( 0.8%) 1149

666-801 A.D.

4 500 GdA-2982 1610±25 1546 (95.4%) 1415 404-535 A.D.

5 640 GdA-2983 2470±25

2713 (35.8%) 26292623 (55.2%) 24462410 ( 1.5%) 23972392 ( 2.8%) 2369

763-419 B.C.

6 710 GdA-2984 2700±25 2850 (95.4%) 2757 900-807 B.C.

7 800 GdA-2985 3030±25 3343 (95.4%) 3161 1393-1211 B.C.

Pol len anal y sis

Sam ples for palynological anal y ses (1 cm3) were col -lected usu ally at 5-10 cm in ter vals; only in the bot tom part ofthe sec tion (900-1080 cm) they were col lected ev ery 20 cm.Sam ples were pre pared us ing the stan dard pro ce dure ofErdtman’s acetolysis (Berglund and Ralska-Jasiewiczowa,1986). Ac cord ing to de gree of con tam i na tion by min eralfrac tion, sam ples were treated with a heavy liq uid (CdI2+KI). Lycopodium tab lets were added to each sam ple to en ablequan ti ta tive anal y sis of microfossil con cen tra tions (Stock-marr, 1971).

Pol len anal y sis was car ried out with the Olym pus BX43light mi cro scope with mag ni fi ca tion of 600×; a larger mag ni -fi ca tion was used to iden tify prob lem atic and small palyno-morphs. For tax o nom i cal iden ti fi ca tion pol len keys (e.g.Beug, 2004) and a ref er ence col lec tion of mod ern pol lenslides were used.

More than 1000 ter res trial pol len grains were countedand identified in each sam ple.

Cal cu la tions and pre sen ta tion of palynological data in asim pli fied per cent age pol len di a gram were per formed withPOLPAL for Win dows soft ware (Nalepka and Walanus,2003). AP+NAP sum was used for per cent age cal cu la tions.The di a gram was di vided into lo cal pol len as sem blage zones(L PAZ) with Con strained Clus ter Anal y sis (CONISS). Todis cuss in ter ac tion of anthropogenic and nat u ral in flu ences,the di a gram was con structed with groups of taxa es tab lishedby Behre (1981), with mod i fi ca tion sug gested by Berglundand Ralska-Jasiewiczowa (1986) and Veski (1998). Pol lencurves of herbs were grouped into three cat e go ries: (1) cul ti -vated crops, (2) weeds and ruderals, and (3) grass land andeco log i cally un de fined plants.

RE SULTS

Chro nol ogy14C and 210Pb dates were used for con struc tion of the

age-depth model for the ana lysed sec tion (Fig. 2). This model was built by means of a poly no mial 2nd de gree curve fit tingin the POLPAL pro gram (Nalepka and Walanus, 2003;Walanus and Nalepka, 2004) and re sulted in draw ing the op -ti mal depth-age curve on the ba sis of cal i brated ra dio car bondates.

Palynological data

Palynological anal y sis was per formed for 128 sam plesfrom the up per part of the sec tion. Four lo cal pol len as sem -blage zones (L PAZ) were dis tin guished (Fig. 3, Ta ble 2).

IN TER PRE TA TION AND DIS CUS SION

Early and mid dle Subboreal (3600–1850 cal.years BC)Quercus-Corylus L PAZ, depth: 1080–870 cm

A vi cin ity of Lake Salêt was densely for ested by multi-spe cies de cid u ous wood land. Oak was the dom i nant tree inthe older part of this pe riod, but it grad u ally de clined in fa -

vour of the in creas ing role of birch. Oak was a com po nent ofsev eral com mu ni ties, es pe cially with ha zel and pine. Due toits high eco log i cal tol er ance, oak de vel oped in di verse hab i -tats, from poor (Quercus petraea) to very rich (Quercus ro-bur) (Szymañski, 2006). From 3567 to 3399 cal. years BC,oak was the most im por tant com po nent of mixed and multi-spe cies de cid u ous for ests in the sur round ings of Lake Salêt.Ac cord ing to Ralska-Jasiewiczowa et al. (2003), there are noclose an a logues to con tem po rary com mu ni ties dom i nated byoak and ha zel. They were formed in re sponse to cy clic occu-pation and ex ploi ta tion of the land by the Neo lithic people.A ris ing pol len curve of Corylus avellana was prob a bly dueto slight open ing of wood lands, which fa voured in ten sive de -vel op ment of their understory. How ever, this pro cess couldhave been also in duced by drier cli mate con di tions (low wa -ter level in lakes and dry phase in peat bogs) be tween 4050and 3650 cal. years BP (¯urek and Pazdur, 1999), and itsgreat po ten tial for veg e ta tion sur vival (Tallantire, 2002). Inthe pol len spec tra from the Lake Salêt profile, Viscum al bumhas been re corded in that time. In the neigh bour hood of thestud ied area pres ence of this con ti nen tal spe cies has beenalso noted (Wacnik, 2009a) and it strongly sug gested warmsum mers, with av er age tem per a ture of the warm est monthabove 15.5°C (Iversen, 1944).

A dis tinct break down in the elm curve was noted in theLake Salêt re gion be tween 2887 and 2563 cal. years BC(Fig. 3). A sim i lar pro cess oc curred also in the Gostynin Lake Dis trict, where it was dated to 2850–2750 cal. years BC(Wacnik et al., 2012b) and the in creas ing role of ha zel wasob served in the fol low ing cen tu ries. The same pat tern wasnoted in the sur round ings of Lake Salêt, where be yond ha zel, in creased sig nif i cance of pine and birch was re corded. Si -mul ta neously with changes in for est com po si tion, dif fer entopen anthropogenic com mu ni ties with ruderal, weed andgrass land taxa de vel oped, and in the youn gest part of this pe -riod ce re als have also ap peared in pol len spec trum (palynolo- gical hu man phase 1).

The prob lem of de cline of Ulmus in the Ho lo cene hasbeen in ten sively dis cussed dur ing the last de cades. Dif fer enthy poth e ses were pro posed, e.g. cli mate change, hu man im -pact and fi nally, spread ing of the so-called “Dutch” elm dis -ease caused by an ascomycete fun gus (Ceratocystis ulmi),and car ried over by bark bee tles Scotylus (e.g. Rackham,

HO LO CENE CHANGES IN VEG E TA TION OF THE MR¥GOWO 53

Fig. 2. Age-depth model of the Lake Salêt pro file based on AMS14C and 210Pb dates.

54 M. SZAL et al.

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1980). Elm re duc tion cor re sponds quite log i cally with suchpatho genic hy poth e sis and it is not very con cor dant with mi -gra tion routes of suc ces sive Neo lithic cul tures. How ever, itseems con vinc ing (Girling and Greig, 1985; Birks, 1986,Ralska-Jasiewiczowa and van Geel, 1998; Peglar, 1993;Innes et al., 2010) that Neo lithic peo ple took ad van tage ofelm dis ease to clear de cid u ous woods grow ing on more fer -tile soils. Pat tern of dis tri bu tion of Ulmus on Pol ish isopollenmaps in di cates that its de cline has been more dif fer en ti ated in time and space than pre vi ously ac cepted (Ralska-Jasiewi-czowa et al., 2003). For in stance, in the Bieszczady Moun -tains elm oc curs around 4400–4200 14C years BP (2450–2250 cal. years BC) only (Ralska-Jasiewiczowa, 1980) andin some low land sites as early as 6000–5700 14C years BP(4050–3750 cal. years BC) (Lata³owa, 1992). De cline ofUlmus is not a syn chro nous event in Es to nia, as the datesrange from 3800 to 3200 cal. years BC, likely due to hu manac tiv ity, con nected with in tro duc tion of ar a ble farm ing rather than by nat u ral fac tors (Saarse and Veski, 2001). In the pol -len di a gram from Lake Salêt a very dis tinct elm de cline isdated to the in ter val 2887–2563 cal. years BC (Fig. 3). Si mul -ta neously with the de cline of Ulmus, Picea abies de vel opedin the vi cin ity of the stud ied site.

Late Subboreal (1850–1200 cal. years BC)Carpinus-Corylus-Quercus-Betula L PAZ, depth:860–770 cm

The most sig nif i cant fea ture of this pe riod was a very dis -tinct spread ing of horn beam in stands of the Lake Salêt re -gion. This pro cess clearly co in cided with de creased impor-tance of hazel as well as lime, elm and oak. Changes in for estcom po si tion were most ev i dently a con se quence of lo calanthropogenic pres sure (a be gin ning of the palynological hu -

man phase 2). More over, hu man ac tiv ity re sult ing in clear ing of some wood land ar eas, pro moted spread ing of horn beam.Horn beam has been well doc u mented as a mod er ate pi o neerspe cies in re cent years. It has rap idly col o nized ar eas af terfall of oak-horn beam woods in the Bia³owie¿a For est (Ber-nadzki et al., 1998).

In the youn ger part of this pe riod a horn beam area has de -creased, and with high prob a bil ity it could re sult from in ten -si fi ca tion of set tle ment at the tran si tion of the Neo lithic andBronze Ages (Manasterski 2009). Cleared ground was usedas pas tures, mead ows, fields and lo cal i ties for set tle ments.Large ar eas of grass lands at that time in di cated pre dom i -nance of an i mal hus bandry rather than cul ti va tion.

Start ing from ca. 1850 cal. years BC a grad ual de creasein im por tance of ha zel was noted. Very dis tinct de cline ofthis spe cies at that time is also re corded in nu mer ous otherpol len di a grams from Po land (e.g. Ralska-Jasiewiczowa etal., 2003), as well as in sev eral sec tions from ad ja cent coun -tries, mainly from Ger many (e.g. Pott, 1986; Brauer et al.,2000; Kubitz, 2000). The on set of this pro cess was de ter -mined to ca. 3400 14C years BP (ca. 1750 cal. years BC) in the Lake Goœci¹¿ (Ralska-Jasiewiczowa et al., 2003), and at ca.3490 14C years BP (ca. 1860 cal. years BC) in lakes from theEifel re gion in Ger many (Brauer et al., 2000). At about 1700cal. years BC for est trans for ma tions oc curred around thePuck Bay in north ern Po land (Miotk-Szpiganowicz, 1997;Uœcinowicz and Miotk-Szpiganowicz, 2003), and some whatsim i larly, Carpinus betulus started to de velop in for est at theex pense of Corylus avellana in the ¯u³awy re gion in theVistula River mouth (Zachowicz et al., 1982, Zachowicz and Kêpiñska, 1987). There are some hints of both a ther mal os -cil la tion to wards a cool ing (Zolitschka, 1992) and an in -crease (al though os cil lat ing) in cli mate hu mid ity (Ralska-Jasiewiczowa and Starkel, 1988), which might be a prob a ble

HO LO CENE CHANGES IN VEG E TA TION OF THE MR¥GOWO 55

Ta ble 2Lake Salêt – description of lo cal pol len as sem blage zones (L PAZ)

Name of L PAZDepth [cm] and age [cal.years] of pol len sam ples

De scrip tion

Pinus-Picea-NAP0–365 cm 2005–981 AD

Dom i na tion of Pinus sylvestris t. (21–47%); rel a tively high fre quency of Picea abies (to 7%); grad ual de crease of Alnus(to 7–8%), Quercus (to ca. 2–3%) and Carpinus betulus (to ca. 1%); rather low val ues of Betula alba t. (be low 23%); lowfre quency of Corylus avellana (to 3,5%), Ulmus (to 1,8%), Tilia cordata (to 2,4%), Fraxinus ex cel sior (to 0,8%), Salix (to1,3%) and Fagus sylvatica (to 0,9%); rel a tively fre quent Juniperus communis; sharp in crease of NAP from 7% to 16%,and then to 48% – high est amount of hu man in di ca tors in the whole di a gram (cul ti vated plants to 16%; ruderals and weeds to 8%).

Carpinus-Betula-Quercus370–770 cm960 AD–1183 BC

Up per bound ary: rapid fall of Betula alba t. be low 18%; rise of Pinus sylvestris t. above 20% and Picea abies to ca. 5%.Ab so lute dom i na tion of Betula alba t. (20–44%); high tri ple cul mi na tion of Carpinus betulus (18%, 12% and 12%); stillhigh val ues of Quercus (8–14%); strong fluc tu a tions of Pinus sylvestris t. (8–30%); low pro por tion of Ulmus (ca. 2%),Tilia cordata (ca. 3%), Fraxinus ex cel sior (ca. 1%), Salix (to 1.5%) and Fagus sylvatica (be low 1%); grad ual de crease ofAlnus from 20–24% to 5–11%; in crease of her ba ceous plants to 12% (cul ti vated plants up to 3%; ruderals and weeds up to 2%).

Carpinus-Corylus-Quercus-Betula780–860 cm1246–1821 BC

Up per bound ary: rapid rise of Betula alba t. above 35% and fall of Corylus avellana.Rapid in crease of Alnus (from 10% to 23%); de crease of Quercus to 8% and Corylus avellana to 6%; low per cent ages ofUlmus (1–2% and Tilia cordata (2–4%); the first cul mi na tion of Carpinus (10%); rel a tively low val ues of Pinus sylvestrist. (15–28%) and Betula alba t. (18–32%); rise of her ba ceous plants to ca. 10% with clear in crease of hu man indicators.

Quercus-Corylus 870–1080 cm1894–3567 BC

Up per bound ary: rise of Carpinus betulus to ca. 7%.Rel a tively high fre quency of Alnus to ca. 22–29%; cul mi na tions of Quercus (26%) and Pinus sylvestris t. (38%) in the bot -tom part of the zone, and then their grad ual de cline; low fre quency of Ulmus to ca. 1% at the depth 960 cm (ca. 2563 BC);al most con stant Tilia cordata curve (ca. 5%); fluc tu a tions of Corylus avellana around 20%; grad ual rise of Carpinusbetulus in the youn ger part of the zone; sys tem atic in crease of her ba ceous plants (NAP) to ca. 5% cor re spond ing with ris -ing val ues of Betula alba t. up to 19%.

rea son for de cline of ha zel. In creas ing cli mate hu mid ity ca.1700 cal. years BC has been re con structed for north ern Brit -ain (Charman et al., 2006) and north ern Nor way (Vorren etal., 2007). From ca. 1500 cal. years BC a ground wa ter ta blerose in mires of North Ire land (Swin dles et al., 2010) and insouth ern Fin land (Väliranta et al., 2007).

A broad spec trum of data from Pol ish flu vial, lake andpeatland en vi ron ments in di cated also an in crease in hu mid ity be tween 4400–4100 and 3500–2900 cal. years BP (2450–2150 and 1550–950 cal. years BC, re spec tively) (Ralska-Jasiewiczowa and Starkel, 1988; ¯urek and Pazdur, 1999;Starkel et al., 2006; Paw³owski et al., 2012). This part of theSubboreal chronozone was con sid ered by Starkel (1990) andStarkel et al. (2006) to have been a wet pe riod, char ac ter izedby more fre quent rainy sea sons. In the Pol ish isopollen mapfor 4000±100 14C years BP (ca. 2050 cal. years BC) Miotk-Szpiganowicz et al. (2004) in di cated that nearly the wholearea of Po land was oc cu pied by Corylus avellana pol len con -tents of 10–15% (west ern, cen tral and north ern Po land,Carpathians Moun tains and Roztocze). The val ues over 15%oc curred in the peri-Baltic area only and be low 10% in theeast ern part of the coun try up to the Podlasie bor der and theCarpathian Foredeep in the Ma³opolska Up land. The laterde creased to be low 5% pro ceeded from SE-E across thewhole coun try and the men tioned au thors as sumed that therewere other rea sons than a con ti nen tal cli mate. It can be con -cluded that de vel op ment of the Early Bronze Age cul tures,prac tic ing rather prim i tive ar a ble ag ri cul ture but broadly de -pend ent on cat tle graz ing (Manasterski 2009) may have con -trib uted to shrink age of ha zel dis tri bu tion.

In the mid dle of this pe riod (ca. 1500 cal. years BC) ar eas with lime and tem po rarily, also the ar eas with elm have de -clined. The elm de cline ca. 1700 years BC was also re cordedin sec tions from the Lakes Mi³kowskie and Wojnowo (Wac-nik et al., 2012a). If these changes are ac cepted to have re -sulted from hu man ac tiv ity, then in creased pol len pro duc tion of Corylus avellana can be ex plained by open ing of the pre -vi ously densely shaded de cid u ous for est by cut ting of elmand lime branches for cat tle fod der. Patches of open hab i tatsbe gan to spread in the area.

Late Subboreal and early Subatlantic (1200 cal.years BC –1000 AD)Carpinus-Betula-Quercus L PAZ, depth:760–370 cm

Deep changes in struc ture of a mixed de cid u ous for esttook place at the very be gin ning of this pe riod, in di cated byrapid spread ing of birch. Veg e ta tion trans for ma tions werecaused both by nat u ral inter gla cial suc ces sion pro voked bycli mate change and by hu man eco nomic ac tiv ity. The dom i -nat ing role of birch and horn beam made for est struc ture dif -fer ent from the pre vi ous one. Horn beam formed pre sum ablythe high est can opy layer that casted shad ows on all lowerstor eys of the for est. This elim i nated ha zel from phytoce-nosis and lim ited its oc cur rence, prob a bly to for est pe riph er -ies only. Horn beam, due to its high abil ity to form suck ersfrom trunk or stumps, could be the main el e ment of re gen er -ated for est, quickly oc cu py ing all larger clear ings (Wacnik et al., 2012b). Max i mum horn beam ex pan sion oc curred about

500 cal. years BC (Fig. 3), just af ter the Lusatian cul ture set -tle ment, which was the most wide spread pre his toric cul turein Po land, char ac ter ized by very high den sity of pop u la tion(God³owski and Koz³owski, 1979). A de cline of this cul tureis re flected in a pol len di a gram from Lake Salêt as the tem po -rary re gen er a tion of for est com mu ni ties, first of pi o neerbirch woods and then of de cid u ous for est with dom i nanthornbeam. The fol low ing pe riod of wood land re duc tion,with ar eas de for ested or thinned by a man be came over grown by var i ous anthropogenic open com mu ni ties and by a helio-philous birch for est. The sec ond, less in ten sive horn beam ex -pan sion started from ca. 200 AD. A his tory of horn beam inthe Ho lo cene in Cen tral Eu rope was strictly con nected withhu man ac tiv ity (see Ralska-Jasiewiczowa, 1964; Ralska-Jasiewiczowa et al., 2004). This spe cies was par tic u larlydev as tated in pe ri ods with in ten sive set tle ment due to fer til -ity of the oc cu pied hab i tats. On the other hand, pe ri ods withre duced anthropogenic pres sure al lowed par tial re gen er a tion of for est com mu ni ties with horn beam, be cause of its great re -gen er a tive abil i ties.

Large ar eas in the vi cin ity of Lake Salêt were still oc cu -pied by oak. Birch for est played a sig nif i cant role in the land -scape, be ing prob a bly sec ond ary semi-nat u ral com mu ni tieswhich were formed in hab i tats trans formed by ex ploi ta tiondur ing ear lier set tle ment stages. An ex pan sion of birch wasalso the most char ac ter is tic fea ture of this pe riod in otherparts of the Masurian Lake Dis trict. For ex am ple, this pro -cess was ev i dent in pol len spec tra from Lake Miko³ajskie(Ralska-Jasiewiczowa, 1966), Woryty (Pawlikowski et al.,1982), Lake Dga³ Wielki (Filbrandt-Czaja, 2000) and LakesMi³kowskie, £azduny and Wojnowo (Wacnik et al., 2012a).Sim i lar de vel op ment of com mu ni ties with dom i nant birchwas re corded in more or less the same time in di a grams fromother parts of Po land, for in stance from the Biebrza RiverVal ley (Balwierz and ¯urek, 1987), Suwa³ki Lake Dis trict(Lake Kluczysko – Wacnik, pers. com ments), cen tral Po land(Biñka et al., 1991), Gostynin Lake Dis trict (Wacnik et al.,2011; Wacnik et al., 2012b) and from Wielkopolska (To-bolski and Okuniewska-Nowaczyk, 1989). In the vi cin ity ofLake Salêt there were also pine and dif fer ent mixed for estswith pine-oak and pine-birch.

Al der grew on wet land hab i tats in the sur round ings ofthe lake and in out skirts of rivers val leys. A rel a tively smallarea was oc cu pied by elm, lime, ash and spruce. Other treeswere rare.

The rise in fre quency of pol len in di ca tors of grass lands,i.e. mead ows and pas tures (the palynological hu man phase 3) in di cates that sur round ings of Lake Salêt have been to someex tent in flu enced by a man. In ten sive ag ri cul ture and a broadex tent of dis turbed soil with high NO3 con tent were confir-med by wide spread pres ence of weeds and ruderals. Open ar -eas were used for cul ti va tion as de noted by con tin u ous pres -ence of Cerealia t. pol len, reg u lar oc cur rence of Secalecereale pol len, and spo radic ap pear ance of Triticum t., Avenat., and Hordeum t. pol len (this is not shown in the pol len di a -gram). Rye, as a wind-pol li nated crop, has higher pol len pro -duc tion and better dis persal pos si bil i ties than other ce re als,and thus its fre quen cies must rep re sent not only lo cal cul ti va -tion but also a re gional back ground (cf. Koff and Pun ning,2002). It is also pos si ble that fields at the edge of Lake Salêt

56 M. SZAL et al.

and ap pear ance of for est graz ing in di ca tors (e.g. Pteridiumaquilinum) point to some what more cat tle-rear ing ac tiv ity inthe area. In thinned and grazed for ests Juniperus communisand Calluna vulgaris occurred.

Late Subatlantic (1000–2005 AD)Pinus-Picea-NAP L PAZ, depth: 365–0 cm

The be gin ning of this pe riod was char ac ter ized by rapidde for es ta tion and by marked in crease in hu man ac tiv ity.With drawal of tree pol len must have been con nected withfor est clear ing un der taken in or der to en large the ar eas of cul -ti vated fields or pas tures and with tim ber ex ploi ta tion, whichis doc u mented in ar chae o log i cal and his tor i cal sources (e.g.Wróblewski et al., 2003; Nowakiewicz, 2006, 2010). Fromaround 1000 AD ex ten sion of hu man eco nomic ac tiv ity star-ted to trans form the nat u ral en vi ron ment in a pro cess per sis tent and con tin ued up to the pres ent time. Ac cord ing to Ralska-Jasiewiczowa (2006) this gen er ated an os ten si ble pic ture re -sem bling the ap proach ing end of the Ho lo cene inter gla cial cy -cle: dis ap pear ance of a de cid u ous for est and first mass sprea-ding of pine, fol lowed by to tal de for es ta tion and oc cu pa tion ofits ter ri tory by open veg e ta tion. Low val ues of tree pol len andpre dom i nance of long-dis tance trans ported pine pol len dem -on strated ex is tence of large open ar eas, which in turn sug -gested pro gres sive de vel op ment of set tle ments.

At the be gin ning of this zone there was a pe riod of in -creased Carpinus betulus pol len per cent ages, which wascon tem po ra ne ous with slightly grow ing hu man eco nomicac tiv ity. A great re gen er a tion abil ity of horn beam al lowedfor its fast ex pan sion in for est un til the early Mid dle Ages.Soon af ter wards, ca. 1250 AD, the ar eas dom i nated by horn -beam shrank grad u ally. Al most to tal elim i na tion of Carpinus betulus from for est stands was prob a bly the ef fect of farm ingin ten si fi ca tion and grow ing de mand for fer tile soils. Di min -ished sig nif i cance of Carpinus betulus in a for est could havebeen also caused by many years’ cat tle graz ing, a con se -quence of which was a for ma tion of well-lit oak-pine forest(Faliñski and Pawlaczyk, 1993).

An im por tance of oak was still sig nif i cant ini tially (981–1033 AD). This could have been caused by se lec tive pro tec -tion of this tree by a man in or der to pro vide acorns, whichcould be stored for up to three years (Weckerly et al., 1989)and used as fod der for pigs, par tic u larly in win ter time.Acorns are a source of a high-en ergy food and now a days, insome sea sons of a year, they may con sti tute up to 50% of thediet of some wild an i mals. Oak leaves are also rich in pro teins (Pe kins and Mautz, 1988; Elowe and Dodge, 1989). It is pos -si ble that acorns were also con sumed by peo ple, just as wasthe case up to re cently among the ab orig i nes of North Amer -ica. Ac cord ing to Pe kins and Mautz (1988) acorn pro duc tioncould have in creased sig nif i cantly by se lec tive fall of trees ina for est and by pro tec tion of ma ture spec i mens. A sud denbreak down in a role of Quercus ca. 940 AD, syn chro nouswith Carpinus betulus de cline and in crease of Pinus sylves-tris t., should be strictly con nected with hu man ac tiv ity.Ralska-Jasiewiczowa (1964) ex plained that oak and horn -beam were par tic u larly dev as tated spe cies in pe ri ods of in -ten sive set tle ment on ac count of fer til ity of the oc cu piedhab i tats. She con cluded also that these trees had great abil ity

to re gen er ate in a com par a tively short time and to spread over cer tain ter ri to ries as one of the main com po nents of anoak-horn beam for est.

Some open ar eas may have be come over grown by wood, in which Picea abies was an im por tant el e ment. Spruce ex -pan sion in the Lake Salêt re gion was dated to ca. 1000 AD, ashas been ob served in some other di a grams from the Masurian Lake Dis trict (e.g. Filbrandt-Czaja, 2000; Wacnik et al.,2012a). An in creas ing pres ence of Calluna vulgaris andPteridium aquilinum, both of which fa vour poorer sandysoils, sug gests open ings in a dry pine for est and sub se quentap pli ca tion of these plots for an i mal hus bandry. Pinus sylves- tris spread most prob a bly on less fer tile, sandy hab i tats,which were cov ered pre vi ously by a mixed co nif er ous for est. Cur rent dis tri bu tion of pine was also con nected with hu manac tiv i ties. Cul mi na tions of Pinus sylvestris t. pol len curveim me di ately af ter each de for es ta tion were al most cer tainlydue to trans port of pine pol len from dis tant ar eas and werealso an ev i dence for spread ing of pine to hab i tats oc cu piedfor merly by an oak-horn beam for est.

At the same time her ba ceous veg e ta tion at tained greatersig nif i cance. Pol len grains of cul ti vated plants oc curred fre -quently. Hith erto un re corded Fagopyrum pol len ap pearedalso in pol len spec tra from the Lake Salêt profile (1116 AD),in di cat ing that buck wheat was prob a bly cul ti vated. This is inagree ment with other Eu ro pean data show ing that buck -wheat, which was na tive to Cen tral Asia and was in tro ducedto Eu rope by the Mongols, was cul ti vated from 12th– 14th

cen tu ries on wards (Speranza et al., 2000; Lata³owa et al.,2007; StanèikaitÅ et al., 2008), al though the ear li est Pol ishre cord, known from the town of Wolin, dated back to 9th–10th

cen tu ries (Alsleben, 1995). Fagopyrum is an in sect-pol li -nated plant which pro duces a small quan tity of pol len that isusu ally underrepresented in pol len spec tra. Re sults of mod -ern pol len mon i tor ing in di cated that buck wheat, wheat andbar ley pol len ap peared in low per cent ages, even when fieldswere lo cated at a small dis tance from the sam pling place(Pidek, 2009). Field and ruderal weeds ap peared in higherper cent ages.

CON CLU SIONS

Pol len anal y sis of the up per part of the sed i men tary se -quence from Lake Salêt al lowed re con struc tion of veg e ta tion changes in the Mr¹gowo Lake Dis trict dur ing Sub-bo real and Subatlantic chronozones of the Ho lo cene (from ca. 3600 cal.years BC).

In the early Subboreal chronozone (3700–2900/2600cal. years BC) oak-pine for est de vel oped, but mixed de cid u -ous wood land with elm, lime and ha zel still oc curred.

Very dis tinct trans for ma tion of a for est co in cided withtran si tion be tween early and mid dle Subboreal chronozone(2900–2600 cal. years BC). This is in di cated by def i nitebreak down of elm, pre ceded by grad ual drop of oak andspread of birch, which started from ca. 3300 cal. years BC.Then, from ca. 2300 cal. years BC, de vel op ment of horn -beam and tem po rary ex ten sion of spruce oc curred. At thattime the first clear ing by hu man communities occurred.

In the late Subboreal chronozone grad ual elim i na tion ofha zel (1800–1200 cal. years BC) was ac com pa nied by ex -

HO LO CENE CHANGES IN VEG E TA TION OF THE MR¥GOWO 57

pan sion of horn beam and pro gres sive de vel op ment of birch.This pro cess should be prob a bly linked with hu man ac tiv ityrather (the Lusatian cul ture) and not with a cli mate change –crop cul ti va tion started from 1800–1700 cal. years BC.

From the end of the Subboreal to the mid dle Subatlanticchronozone (1200 cal. years BC–1000 AD) a max i mumspread ing of birch and horn beam for est oc curred. Two pe ri -ods of horn beam ex pan sion were re corded from that time, at700–400 cal. years BC and 200–1000 AD. From ca. 500 cal.years BC dis tinct spread ing of anthropogenic com mu ni ties(grass lands, cul ti vated fields, ruderal com mu ni ties) hasstarted.

Ex ten sive wood land clear ances and oc cur rence of vastar eas in hab ited by peo ple and ex ploited by them eco nom i -cally and ag ri cul tur ally started from ca. 1000 AD. The ar easof all trees, with ex cep tion of pine and spruce, were at thattime sub stan tially reduced.

A palynological study con sid er ing ar chae o log i cal andhis tor i cal in for ma tion, which will pro vide a more de tailed re -con struc tion of hu man im pact on veg e ta tion in the sur round -ings of Lake Salêt, will be pub lished in a separate paper.

Ac knowl edge ments

The study was fi nanced by the Pol ish Min is try of Sci ence andHigher Ed u ca tion through the pro ject no. NN 304 280540.

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