Geo log i cal Quar terly, 2014, 58 (2): 235–250 DOI: http://dx.doi.org/10.7306/gq.1158
How to re solve Pleis to cene strati graphic prob lems by dif fer ent meth ods?
A case study from east ern Po land
S³awomir TERPI£OWSKI1, *, Tomasz ZIELIÑSKI2, Jaros³aw KUSIAK1, **, Irena A. PIDEK1, Piotr CZUBLA3, Anna HRYNOWIECKA4, Anna GODLEWSKA1, Pawe³ ZIELIÑSKI1 and Marzena MA£EK5
1 Maria Cu rie-Sk³odowska Uni ver sity, De part ment of Geoecology and Palaeo ge ogra phy, Kraœnicka 2c,d, 20-718 Lublin, Po land
2 Adam Mickiewicz Uni ver sity, In sti tute of Ge ol ogy, Maków Polnych 16, 61-606 Poznañ, Po land
3 £ódŸ Uni ver sity, Lab o ra tory of Ge ol ogy, Narutowicza 88, 90-139 £ódŸ, Po land
4 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Ma rine Ge ol ogy Branch, Koœcierska 5, 80-328 Gdañsk, Po land
5 Geo log i cal En ter prisePOLGEOL S.A., Lublin Of fice, Budowlana 26, 20-469 Lublin, Po land
Terpi³owski, S., Zieliñski, T., Kusiak, J., Pidek, I., A., Czubla, P., Hrynowiecka, A., Godlewska, A., Zieliñski, P., Ma³ek, M., 2014. How to re solve Pleis to cene strati graphic prob lems by dif fer ent meth ods? A case study from east ern Po land. Geo log i - cal Quar terly, 58 (2): 235–250, doi: 10.7306/gq.1158
Dif fer ent meth ods have been used to de ter mine the strati graphic po si tion of Pleis to cene al lu vial de pos its, par tic u larly flu vial inter gla cial de pos its. Near-sur face de pos its of a me an der ing river, de vel oped in point-bar and ox bow lake fa cies, in the Samica River val ley (near £uków, east ern Po land) have been in ves ti gated. The fos sil val ley is in cised into the till plain and the outwash. The flu vial suc ces sion is lo cally over lain by solifluction de pos its. All the de pos its un der went sedimentological anal y sis. The petrographic com po si tion of basal till oc cur ring in the vi cin ity of a fos sil val ley was de ter mined with the method of in di ca tor er rat ics. Flu vial de pos its were ex am ined by pol len anal y sis and plant macrofossil anal y sis of ox bow lake fa cies.
Ab so lute dat ing meth ods were ap plied to the de pos its (thermoluminescence meth ods: TL and ad di tion ally IRSL).
Lithological dif fer ences be tween flu vial and the sur round ing glaciofluvial de pos its were iden ti fied and their lithostratigraphic po si tion as signed. Petrographic anal y sis of till and palaeobotanical anal y ses of ox bow lake fa cies gave com pat i ble re sults.
Flu vial de pos its were formed af ter the Sanian 2/Elsterian Gla ci ation, dur ing the Mazovian/Holsteinian Inter gla cial. Lu mi nes - cence dat ing of the flu vial de pos its by the TLMAX method yielded the most rel e vant re sults (412–445 ka), which in di cate that these de pos its were formed dur ing the end of the MIS 12 and be gin ning of the MIS 11 stage.
Key words: chronostratigraphy, geo chron ol ogy, inter gla cial me an der ing river, Pleis to cene, Mazovian/Holsteinian, eastern Po land.
INTRODUCTION
Inter gla cial flu vial de pos its are im por tant for Pleis to cene stra tig ra phy. In Cen tral-East ern Eu rope, a re gion gla ci ated sev - eral times, the pre-Ho lo cene flu vial de pos its have been in ves ti - gated in bore hole cores only. Their strati graphic po si tion was de ter mined by palaeobotanical anal y ses of biogenic and clastic de pos its, their su per po si tion on till units, and their ages de ter - mined by thermoluminescence dat ing of clastic de pos its (e.g., Lindner et al., 1982; Krzyszkowski, 1992; Marks and Pavlovskaya, 2003; Albrycht, 2004). We re gard such in ter pre - ta tion of inter gla cial or i gin as in com plete if fa cies anal y sis is lack ing. Un con sol i dated de pos its sam pled from bore hole cores can not be stud ied sedimentologically.
The aim of this pa per is to de scribe flu vial de pos its and to de ter mine their strati graphic po si tion, fo cus sing on a unique,
near-sur face de posit of a me an der ing river in the Samica val ley near £uków in east ern Po land. This is the first re port of these de pos its. The fol low ing meth ods were used: (1) lithofacies anal - y sis of the flu vial suc ces sion, (2) petrographic anal y sis of till from the till plain dis sected by the palaeo-river, (3) palaeobotanical (pol len and plant macrofossil) anal y ses of biogenic ox bow lake de pos its, and (4) lu mi nes cence dat ing of clastic chan nel de pos its.
The ques tions ad dressed in this pa per are: (1) Which lithological fea tures can be re garded as in di ca tors of inter gla cial flu vial de po si tion? (2) Can the petrographic char ac ter of till be used to de ter mine the strati graphic po si tion of flu vial de pos its in cised into the till plain? (3) Which palaeobotanical fea tures of biogenic ox bow lake fa cies may be used to re cog nise its strati - graphic po si tion? (4) Which thermoluminescence method is most use ful for ab so lute dat ing of the flu vial de pos its?
SITE INVESTIGATED
The Pleis to cene sur face suc ces sion of the £uków re gion is tra di tion ally clas si fied as the youn gest de pos its of the Mid dle
* Corresponding author, e-mail: terpis@poczta.umcs.lublin.pl
** Deceased
Received: June 10, 2013; accepted: December 23, 2013; first published online: March 25, 2014
Pol ish Com plex: the Odranian Gla ci ation and Wartanian Stadial (cf. Terpi³owski, 2001; Ma³ek, 2004; Ma³ek and Buczek, 2009; Lindner and Marks, 2012), which are an a logues of the Drenthe and Warthe units of the late Saalian of West ern Eu - rope (Fig. 1). The Wartanian Stadial ice-sheet limit is the bound ary be tween two ar eas of dis tinctly dif fer ent geo mor phol - ogy (Fig. 2). The north ern area is a mor pho log i cally and lithologically di verse mar ginal zone of the Wartanian Stadial ice sheet, formed by prox i mal outwash, eskers and kames. The south ern area is a large outwash plain of the Wartanian Stadial ice sheet. It passes into the val ley outwash trains of the up per reaches of the Krzna River and Bystrzyca Pó³nocna River with its main trib u tary – the Samica River. These outwash de pos its fill the val leys, which cut into the flat till plain of the Odranian Gla ci ation.
The flu vial de pos its in ves ti gated (unit C) of the Samica River (Kolonia Domaszewska site) fill the fos sil val ley in cised both into till (unit A) and outwash grav elly sands (unit B). Flu vial unit C is lo cally over lain by re de pos ited gla cial de pos its (unit D) (Figs. 2B and 3). The com plete flu vial suc ces sion (unit C) is as fol lows: sands and grav els ® sands and silts (sub unit C-1) ® or ganic and min eral de pos its (sub unit C-2; Fig. 3).
MATERIAL AND METHODS
SEDIMENTOLOGICAL ANALYSIS
De pos its of all Pleis to cene units (A–D, Fig. 3) were in ves ti - gated us ing sedimentological anal y sis. Units A, B, D and sub - unit C-1 were stud ied in the field. Sub unit C-2 was stud ied from undeformed core ob tained us ing an Eijkelkamp corer. The tex - ture and struc ture of all units were ana lysed, to gether with the thick ness, shape and ex tent of depositional bod ies (lithofacies) and con tacts be tween them. Lithofacies were la beled us ing Miall (1978) and Krüger and Kj³r (1999) codes with some mod - i fi ca tions (Zieliñski and Pisarska-Jamro¿y, 2012; Ta ble 1). The ori en ta tions (dips and dip di rec tions) of beds and cross-laminae
were mea sured to in fer palaeochannel mor phol ogy and flow di - rec tion, while ori en ta tions of the lon gest gravel axes were used to in ter pret the till or i gin and di rec tion of ice-sheet ad vance.
Duc tile and brit tle de for ma tion struc tures were noted and their di men sions and ori en ta tions mea sured.
PETROGRAPHIC ANALYSIS
Petrographic anal y sis was car ried out only for the basal till (unit A) of the till plain (Figs. 2B, 3 and 4, log 1). This method is com monly used to ana lyse in di ca tor er rat ics in Ger many and Po land and to iden tify their source ar eas (e.g., Meyer, 1983;
Vinx et al., 1997; Hoffmann and Meyer, 1999; Czubla, 2001, 2006; Lüttig, 2005; Górska, 2006; Górska-Zabielska, 2008;
Czubla et al., 2010a, b). A sam ple con tain ing ap prox i mately 1000 clasts of the coarse gravel frac tion (>20 mm in di am e ter) was ex tracted from a till-bed ex posed in the pit. In di ca tor rocks of pre cisely iden ti fied Fennoscandian prov e nance were sep a - rated and ana lysed us ing Lüttig’s method (1958), mod i fied by Vinx et al. (1997) and Czubla (2001). Each in di ca tor rock was as signed with geo graph ical co or di nates of the mid-point of its source area in Fennoscandia, and these (al ti tudes and lon gi - tudes sep a rately) were added and av er aged. The re sult was a geo graph ical lo ca tion of the mid-point of the source ar eas of in - di ca tor rocks in the till-bed stud ied – the The o ret i cal Boul der Cen tre (TBC; Lüttig, 1958), per mit ting in di vid ual sam ples ex - tracted from gla cial de pos its to be com pared. Based on crys tal - line (ig ne ous and meta mor phic) er rat ics only to avoid the ef fect of elim i na tion of less re sis tant sed i men tary rocks, the TBC was cal cu lated and com pared with the TBCs as signed for tills in the South Podlasie Low land. The pro por tions of dif fer ent rock groups were de ter mined and, fol low ing the pro ce dure de - Fig. 1. Cor re la tion of glaciations and interglacials in Po land
(Ber et al., 2007) with their equiv a lents in West ern Eu rope (Co hen and Gibbard, 2010)
Code De scrip tion
Tex ture
T silts
ST silty sands
S sands
SG grav elly sands
G gravels
GS sandy gravels
GSD diamictic sandy gravels
D diamicton (till)
DS sandy diamicton
C or ganic or or ganic-clastic de posits (peats, gyttja) Struc ture
m mas sive
(m1) ma trix-sup ported, gravels con tent <15% (for till only) h hor i zon tal lam i na tion/strat i fi ca tion
r rip ple cross-lam i na tion
f flaser lam i na tion
t trough cross-strat i fi ca tion l low-an gle cross-strat i fi ca tion x cross lam i na tion/strat i fi ca tion (in gen eral)
e ero sional scour fill
s strat i fied (for diamicton only)
d de formed
T a b l e 1 Lithofacies code sym bols used in this study
scribed by Smed (1993), a map of the dis tri bu tion of in di ca tor er rat ics was drawn.
PALAEOBOTANICAL ANALYSES
Palaeobotanical anal y ses in cluded pol len anal y sis and plant macrofossil anal y sis. They were based on the core (SO1) taken from a depth in ter val of 1.05–3.65 m us ing an Eijkelkamp corer
(sub unit C-2; Figs. 5 and 6). The core was sam pled and ana lysed ev ery 5–10 cm, de pend ing on changes in pol len spec tra.
POLLEN ANALYSIS
Ma te rial for pol len anal y sis was ob tained us ing hy dro flu oric acid method. Sam ples were treated with 10% HCl to re move car - bon ates, then boiled with 3.5% KOH. The min eral frac tion was re moved us ing 40% HF. The or ganic frac tion was sub jected to How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland 237
Fig. 2. The £uków area
A – lo ca tion in the con text of the ice-sheet max i mum ex tent of the Wartanian/Warthe Stadial of the Odranian/Drenthe Gla ci ation (af ter Marks, 2004); B – geomorphological sketch (ac cord ing to Terpi³owski, 2001; Ma³ek, 2004; Ma³ek and Buczek, 2009)
Fig. 3. Sche matic cross-sec tion through the Samica River val ley in the Kolonia Domaszewska For lo ca tion see Fig ure 2
Fig. 4. Sed i men tary logs of units A and B in the Kolonia Domaszewska For their lo ca tion see Fig ure 3; for lithofacies sym bols see Ta ble 1
How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland239
l i s s o f e h t
f
o s t i s o p e d
l
a i v u l F
.
5
.
g i
F SamicaRive rval leyintheKoloniaDomaszewska
A–de pos itso ftwopalaeochannelsandlo ca tiono fsed i men tarylogs ;B –planformviewo fthepalaeochannels
Erdtman’s acetolysis, the sporomorphs ob tained were stained with acid fuchsine and washed with pure glyc er ine. Pol len spec - tra were counted on at least two slides. Usu ally 600–900 pol len grains of trees and shrubs (AP) were counted in sam ples with good fre quency of sporomorphs. In sam ples with few sporomorphs – at least 300–400 grains of AP+NAP were counted. The re sults of pol len anal y sis of 33 sam ples are shown in a per cent age di a gram, pre pared us ing POLPAL soft ware (Nalepka and Walanus, 2003). The cal cu la tions of pol len and spore per cent ages were based on the sum of pol len grains of trees and shrubs (AP) and of ter res trial herbs and dwarf shrubs (NAP). The per cent ages of aquatic and lakeshore veg e ta tion pol len of Pteridophyta and Bryophyta spores, al gae, re de pos ited and non-de ter mined taxa were cal cu lated in re la tion to the sum AP+NAP+given taxon. The pol len suc ces sion is di vided into lo - cal pol len as sem blage zones (LPAZs) dis tin guished us ing cri te - ria pub lished by West (1970) and Janczyk-Kopikowa (1987). The names of the zones are de rived from these taxa, which are pre - dom i nant in or typ i cal of a par tic u lar zone.
PLANT MACROFOSSIL ANALYSIS
Sam ples for anal y sis of plant macroremains (29 sam ples) were taken in cor re la tion with ones used for pol len anal y sis. All sam ples were sub jected to mac er a tion us ing a 10% so lu tion of KOH and de ter gents. 150 ml of sed i ment was soaked in wa ter for ca. 24 hours and then boiled with KOH added. Af ter the sed i - ment was boiled to a pulp, the sam ples un der went wet sieve anal y sis us ing a 0.2 mm mesh sieve. The ma te rial re main ing on the sieve was sorted un der a mag ni fy ing glass. All plant re - mains qual i fy ing for iden ti fi ca tion were iso lated and placed in a mix ture of glyc er ine, wa ter and ethyl al co hol in ra tio of 1:1:1, with thymol added. The ma te rial was stored in sep a rate small
“boxes”. The iso lated plant re mains were de ter mined to spe cies level, as far as was pos si ble, con sid er ing the con di tion of the pre served ma te rial (cf. Hrynowiecka and Szymczyk, 2011;
Stachowicz-Rybka, 2011). Sam ples from depths of 105, 120, 125 cm and 140–145 cm, were bar ren or con tained only sin gle
un iden ti fi able frag ments of plant tis sues. The plant macroremains de ter mined were in cluded into lo cal macrofossil as sem blage zones (LMAZs) and cor re lated with LPAZs.
LUMINESCENCE DATING
The lu mi nes cence age of de posit is given by the ra tio of the equiv a lent dose to the dose rate. The equiv a lent dose is de fined as the ir ra di a tion dose ab sorbed by a sam ple in the lab o ra tory, as sum ing that its lu mi nes cence in ten sity is the same as in nat u - ral con di tions. The dose rate is de fined as the en ergy of ion iz ing ra di a tion ab sorbed by a sam ple in a unit of time (year, mil len - nium).
The age of six sandy-silty sam ples de rived from point-bar fa cies (sub unit C-1; for their lo ca tion see Figs. 5 and 6) was es ti - mated by thermoluminescence (TL). Al though this method is not thought to pro vide good re sults for de pos its older than 300–400 ka (Frechen et al., 1999; Bluszcz, 2000), we use it be - cause some stud ies (Berger et al., 1992; £anczont et al., 2011;
Kusiak et al., 2013) show that it is pos si ble to ac cu rately date de pos its up to 500–800 ka. For con trol, two sam ples from log 1 were dated by in fra red light stim u lated lu mi nes cence (IRSL), which al lows dat ing of de pos its up to 300 ka (e.g., Yi et al., 2012).
Ma te rial for anal y sis was pre pared and mea sure ments car - ried out in a room lit with Kai ser Spec tral 590 lamps. In or der to de ter mine the equiv a lent dose (ED) the 45–56 mm polymineral frac tion was sep a rated by wet siev ing, the min eral ma te rial be - ing treated with 10% HCl and 30% H2O2.
For TL dat ing the min eral grains were ir ra di ated with a 60Co g source to 5000 Gy in the In sti tute of Nu clear Chem is try and Tech nol ogy in War saw. Af ter ir ra di a tion the sam ples were stored for three months. Be fore the TL mea sure ments they were pre heated at 160°C for 3 hours, the glow curves be ing re - corded us ing a RA’94 thermoluminescence one-po si tion reader (pro duced by Mikrolab Kraków, Po land) with an EMI 9789 QA photomultiplier. A BG-28 op ti cal fil ter (380–500 nm) was used Fig. 6. Sed i men tary logs of the flu vial units in the Kolonia Domaszewska
For their lo ca tion and ex pla na tions see Fig ures 4 and 5; for lithofacies sym bols see Ta ble 1
(Berger et al., 1992). The sam ples were heated up to 400°C at the rate of 10°C/sec in an ar gon at mo sphere. To de ter mine the equiv a lent dose the to tal-bleach tech nique was used. Lu mi nes - cence in ten sity was de ter mined in two dif fer ent ways. Two re - gions un der the glow curve were es tab lished at the light sum:
(1) the 10°C wide re gion of the glow peak (TLMAX) (Kusiak, 2008; £anczont et al., 2011; Kusiak et al., 2013), (2) the 100°C wide re gion (270–370°C; TLINT) con tain ing the glow peak (Frechen, 1992). The pla teau test was car ried out; for all sam - ples the glow peak oc curred within the pla teau.
IRSL mea sure ments were made fol low ing the sin gle aliquot re gen er a tion (SAR) pro ce dure (Murray and Wintle, 2000;
Wallinga et al., 2000). The RisÝ TL-DA-20 au to matic reader was used with the fil ter set (320–480 nm): Schott BG-39 and Corn ing 7-59. Ta ble 2 de scribes the two dat ing pro ce dures:
pIRIR290 – lu mi nes cence read ing at a tem per a ture of 50°C and then at 290°C (Thiel et al., 2011) and MET-pIRIR – lu mi nes - cence read ing at a tem per a ture of 50°C, and ev ery 50°C up to 300°C (Li and Li, 2011).
The dose rate was de ter mined by means of gamma spec - tros copy. Sta tion ary spec trom e ters Mazar-01 and Mazar-95 with scin til la tion probes (pro duced by Polon-Izot Milanówek, Po land) and con tain ers of Marinelli type with a vol ume of 470 cm3 were used. The mea sure ment time for one sam ple was 80,000 s. Cor rec tions were made for cos mic ra di a tion (Prescott and Hutton, 1994) and for de posit mois ture at the
18% level (Berger, 1988). The ef fi ciency fac tor of al pha ra di a - tion in lu mi nes cence in duc ing was used (Benea et al., 2007).
The con cen tra tions of ra dio iso topes were con verted into ab - sorbed dose rates for a, b and g ra di a tion, based on data pub - lished by Adamiec and Aitken (1998; Ta ble 3).
RESULTS
SEDIMENTOLOGICAL ANALYSIS UNIT A
Unit A is 3 m thick and built the east ern slope of the Samica River val ley (Figs. 2B and 3). Mas sive diamicton – lithofacies Dm(m1) – con tains a few elon gated sandy clasts and rare grav - els dis persed within the ma trix (Fig. 4, log 1). Gravel fab ric is very good (S1 = 0.7163). The di rec tional dis tri bu tion is sym met - ri cal, with a dis tinct N–S mode (mean vec tor = 171°). The basal con tact with sandy-grav elly glaciofluvial de pos its is partly deformational. Some wedges filled with the diamicton are bor - dered by shear planes (nor mal faults and flex ures). Their strike is W–E (mean vec tor = 85°), i.e. trans verse to the ori en ta tion of elon gated grav els within the diamicton.
Diamicton of unit A dis plays fea tures typ i cal of basal till of lodge ment type (Dreimanis, 1989). The mas sive struc ture, How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland 241
pIRIR290 MET-pIRIR
Step Treat ment Ob served Step Treat ment Ob served
1 2 3 4 5 6 7 8 9 10
Given dose, Di
Pre heat, 320°C for 60 s IRSL mea sure ment, 200 s at 50°C IRSL mea sure ment, 200 s at 290°C
Give test dose, DT
Pre heat, 320°C for 60 s IRSL mea sure ment, 200 s at 50°C IRSL mea sure ment, 200 s at 290°C IRSL mea sure ment, 100 s at 325°C
Re turn to 1
Lx
Lx
Tx
Tx
1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18
Given dose, Di
Pre heat, 320°C for 60 s IRSL mea sure ment, 100 s at 50°C IRSL mea sure ment, 100 s at 100°C IRSL mea sure ment, 100 s at 150°C IRSL mea sure ment, 100 s at 200°C IRSL mea sure ment, 100 s at 250°C IRSL mea sure ment, 100 s at 300°C
Give test dose, DT
Pre heat, 320°C for 60 s IRSL mea sure ment, 100 s at 50°C IRSL mea sure ment, 100 s at 100°C IRSL mea sure ment, 100 s at 150°C IRSL mea sure ment, 100 s at 200°C IRSL mea sure ment, 100 s at 250°C IRSL mea sure ment, 100 s at 300°C IRSL mea sure ment, 100 s at 325°C
Re turn to 1
Lx50
Lx100
Lx150
Lx200
Lx250
Lx300
Tx50
Tx100
Tx150
Tx200
Tx250
Tx300
T a b l e 2 De scrip tion of the pIRIR290 and MET-pIRIR dat ing pro ce dures of the IRSL method (Thiel et al., 2011; Li and Li, 2011)
Sam ple Depth
[m] Sam ple No.
Lub- K
[Bq/kg] U
[Bq/kg] Th
[Bq/kg]
Dose rate Dr
[Gy/ka]
SPB-1 SPB-2 SPB-3 SPB-4 SPB-5 SPB-6
1.4 3.4 2.4 3.2 3.4 2.0
5181 5183 5186 5188 5189 5196
362 ± 16 351 ± 18 250 ± 13 387 ± 17 395 ± 21 116 ± 6
21.6 ± 1.9 31.9 ± 2.9 15.1 ± 1.4 28.1 ± 2.5 41.8 ± 3.1 10.8 ± 1.0
25.3 ± 1.3 26.5 ± 1.4 19.3 ± 1.1 30.9 ± 1.5 28.6 ± 1.4 6.7 ± 0.4
2.49 ± 0.12 2.78 ± 0.14 1.90 ± 0.15 2.90 ± 0.15 3.39 ± 0.16 1.02 ± 0.09
T a b l e 3 Con cen tra tions of ra dio iso topes (K, U, Th) and val ues of dose rate (Dr)
deformational con tact with un der ly ing glaciofluvial de pos its, and char ac ter of deformational struc tures de rived from si mul ta - neous lodge ment and shear ing along an ice-sheet sole (cf.
Boulton and Hind marsh, 1987; Hart and Boulton, 1991; Van der Meer et al., 2003). The well-de vel oped gravel fab ric to gether with trans verse ori en ta tion of deformational struc tures sup port this ge netic in ter pre ta tion. These in di cate ice-sheet ad vance from the North.
UNIT B
De pos its of unit B form a 600–800 m wide tract, ori ented NNW-SSE (Figs. 2 and 3). It is the old est ter race level in the pres ent-day Samica River val ley. Fine-grained sands with sandy-grav elly intrabeds pre vail in unit B (Fig. 4, log 2). Trough cross-strat i fi ca tion (lithofacies St, SGt), mainly of large scale, is the most com mon depositional struc ture. The larg est troughs (deeper than 1 m and lon ger than 10 m) usu ally con tain the com pound infill. In places the cosets of cross-laminae are di - vided by re ac ti va tion sur faces. In other cases, the struc ture changes within the sandy infill: low-an gle cross-strat i fi ca tion (lithofacies Sl) is over lain by hor i zon tal strat i fi ca tion (lithofacies Sh). The lower part of the trough is filled with sandy-clayey (diamictic) gravel with mas sive struc ture (lithofacies GSDm), whereas the up per part is made up of cross-strat i fied grav elly sand (lithofacies SGt). The beds of mas sive sand (lithofacies Sm) and gravel (lithofacies Gm), 40–50 cm thick, are a sec ond - ary lithofacies in unit B. In the up per part an ice-wedge cast 70 cm long was found.
We in ter pret unit B as the sed i men tary re cord of a val ley sandur – elon gated outwash con fined by val ley slopes. It de - rived from the re treat of the ice sheet which formed the sur - round ing till plain. Lat eral shift ing as well as ex ten sive aggradation of braided chan nels were in hib ited in this con fined flu vial en vi ron ment. There fore the chan nel bed un der went fre - quent ero sion and abun dant troughs were formed. The trough cross-strat i fied beds St thin ner than 0.5 m were linked with pro - cesses of lo cal ero sion and de po si tion in sep a ra tion zones lo - cated dis tally to the three-di men sional dunes. The larger troughs are in ter preted as the re cord of pools in the cen tral ar - eas of high-en ergy chan nels (Siegenthaler and Huggenberger, 1993; Marren et al., 2009). Their fill ing with sed i ment took place in a few phases, most prob a bly dur ing suc ces sive floods (see Olsen and Andreasen, 1995). Re ac ti va tion sur faces in di cate fre quent, short-term pulses of melt wa ter dis charge. Ver ti cal suc ces sions Sl ® Sh within large-scale troughs prove the de - po si tion from tran si tional and super criti cal cur rents which were gen er ated by high flow ve loc ity. Diamictic grav els at the base of some com pound infills sug gest that pow er ful ab la tion floods (with ero sion of pools) were con nected with flow-till surges which un der went ini tial flu vial redeposition (de po si tion of GSDm lithofacies; Pisarska-Jamro¿y and Zieliñski, 2014). This lithofacies is ev i dence for ice-sheet mar gin prox im ity (cf. Aitken, 1998). The beds of mas sive sand and gravel de rived from abrupt aggradation are thought to rep re sent the first phases of wan ing floods. Di rec tional data of cross-beds show that proglacial meltwaters flowed to wards the SSW (mean az i muth
= 218°). Palaeocurrent dis tri bu tion cov ers 180° with three main modes (to wards the SSW, SSE and ESE) which re flect ori en ta - tion of chan nels within a braided sys tem. Lithofacies as so ci a - tion St, Gt, Sh, gen er ally sim i lar to the stud ied unit B, has been found by Dobracki and Krzyszkowski (1997) in prox i mal Pleis to - cene outwash in NW Po land.
UNIT C
This is the main pack age of de pos its in ves ti gated be cause it con tains or ganic beds and an inter gla cial or i gin is in ferred. It
in cludes two flu vial sub units de rived from: an ac tive chan nel (sub unit C-1) and an ox bow lake (sub unit C-2; Figs. 3 and 5).
Sub unit C-1. This sub unit is com posed of sand, silty sand and silt (com monly oc cur ring as rhythmites), with sub or di nate grav elly sand (Figs. 5 and 6). These de pos its fill two stacked palaeochannels 50–70 m wide and up to 8 m deep. The up per palaeochannel is partly in cised in the lower one. The pack ages of sand beds are char ac ter ized by low-an gle (<15°) uni form dip (lithofacies Sl), trans verse to the palaeochannel axes. In clined par al lel lam i na tion pre dom i nates in the beds but there is also mas sive struc ture as well as pla nar cross-strat i fi ca tion where laminae dip op po site to the bed in cli na tion. There fore, these are pack ages of ep si lon cross-strat i fi ca tion (ESC) type de rived from point bars. Par al lel, in clined lam i na tion in sand is a re cord of de - po si tion on the point-bar plat form which gently sloped to wards the thalweg. Sandy-silt beds within in clined beds (lithofacies STl) typ i cally show par al lel lam i na tion, but flaser lam i na tion has been also noted. The fre quency of sandy-silt and silt com po nents in - creases to wards the tops of palaeochannel infills. Fin ing-up suc - ces sions 30–70 cm thick are pres ent within palaeochannel infills.
They start from erosively-based coarse sand with gran ules (lithofacies SGl or SGp lithofacies) over lain by fine sand with par - al lel lam i na tion (lithofacies Sl) and then by lam i nated sandy silt (lithofacies TSh or TSl).
Chan nel de pos its ar ranged in ep si lon cross-strat i fi ca tion (ESC) in di cate that palaeochannels were highly sin u ous; this was a typ i cal me an der ing river with bends of small ra dius (Miall, 1996). In terms of flu vial fa cies mod els, the de pos its stud ied are re garded as the sed i men tary re cord of a low-en ergy me an der ing river, as the chan nel fa cies stud ied com prises an as so ci a tion of fine-grained sand beds to gether with silty ones, i.e. ep si lon cross-strat i fi ca tion (ESC) can be iden ti fied in this case with in - clined heterolithic strat i fi ca tion (IHS) sensu Thomas et al. (1987).
Sim i lar fine-grained de pos its of highly sin u ous al lu vial chan nels have been re ported by Ed wards et al. (1983), Gibling and Rust (1987), Smith (1987) and Wood (1989). An other typ i cal me an - der ing-river fea ture of the suc ces sion stud ied is the pres ence of a thick (1 m or more) silty pack age cap ping the palaeochannel sed - i men tary pro file (cf. Blakey and Gubitosa, 1984). Di rec tional data of bed ding and strat i fi ca tion/lam i na tion is also an im por tant tool in en vi ron men tal in ter pre ta tion. Gen er ally, the river flowed to the NNE (mean vec tor = 327°), i.e. op pos ing to the pre vi ous outwash sys tem (unit B). Dip az i muths show a spread of 360° with polymodal dis tri bu tion which is typ i cal of highly sin u ous (me an - der ing) chan nels. The three main di rec tions seen in the cur rent rose di a gram re flect pri mary chan nel di rec tions: WWN and ESE rep re sent point-bar lat eral ac cre tion, and N is con nected with the main flow in the thalweg. All these fea tures sug gest a me an der - ing river in a tem per ate cli mate.
Sub unit C-2. The ox bow of the youn ger palaeochannel is filled with about 2 m of or ganic and clastic de pos its (Figs. 5 and 6). The sed i men tary suc ces sion is as fol lows: mas sive silt (lithofacies Tm) ® mas sive or ganic de pos its (lithofacies Cm) – gyttja with peat in ter ca la tions in the lower part, peat with gyttja in ter ca la tions in the up per part ® sandy strat i fied diamicton (lithofacies DSs) with mas sive gyttja intrabeds (lithofacies Cm) (Fig. 6). The lithologies and su per po si tion of these mem bers in sub unit C-2 sug gests de po si tion in an oligotrophic/mesotrophic lake which un der went pro gres sive eutrophization and fi nally was filled with sed i ment of unit D.
UNIT D
In the tran si tion zone be tween the palaeochannel and the till plain, the chan nel de pos its are cov ered by a unit of sandy, strat - i fied diamicton, which is up to 2 m thick in the ax ial part of the palaeochannel (Figs. 3 and 6). It con sists of ir reg u lar, de formed beds of clayey sand and gravel with poor fab ric (mean vec tor =
How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland 243
Fig. 7. Source ar eas of in di ca tor er rat ics rec og nized in the Kolonia Domaszewska till
The cir cle’s area cor re sponds to the per cent age of er rat ics in an ana lysed stone sam ple; graphic pre sen ta tion method (cir cle map) af ter Smed (1993): 1 – ngermanland gran ite-gneiss; 2 – land and/or Nystad Pyterlite; 3 – land gran ite, Haga gran - ite, land Rapakivi, land aplite gran ite, land gran ite por phyry; 4 – red Bal tic quartz por phyry; 5 – Sala gran ite; 6 – Stock - holm gran ite; 7 – Glöte por phyry; 8 – sen, Bredvad and K¯tilla por phy ries, Garberg gran ite; 9 – Öje diabase and melaphyre, Dala sand stone, Digebergs sand stone and con glom er ate;, 10 – Venjan por phyry; 11 – Siljan gran ite, Siljan Rapakivi, M¯nsta por phyry; 12 – red and brown Graversfors gran ites, Östgöta gran ites; 13 – red Sm¯land gran ites, Vislanda gran ite, Sm¯land por phy ries; 14 – Kalmarsund and Tessini sand stones; 15 – Karlshamn and Spinkam¯la (Halen) gran ites; 16 – Kullaite, Scolithos and Hardeberga sand stones; 17 – Ham mer and Vang gran ites, Born holm gneiss es; 18 – red Cam brian sand - stones; 19 – red Or do vi cian lime stones; 20 – Beyrichia lime stone
94°). These al ter nate with dis con tin u ous sand lay ers of crude strat i fi ca tion. Diamictic load casts (up to 1.5 m in am pli tude), uni formly in clined folds and frac tures with un der ly ing flu vial sands are the most abun dant de for - ma tion struc tures.
Such fea tures are typ i cal of slope solifluction de pos - its (Steijn et al., 1995). The ori en ta tions of elon gated grav els sug gests that massflow redeposition took place from the till plain bor der ing the fos sil val ley to the east.
PETROGRAPHIC ANALYSIS
Crys tal line rocks (64.78%) are pre dom i nant in the group of Fennoscandian rocks of the basal till. Among these, in di ca tor er rat ics are quite com mon – 15.66%.
These are mostly rocks from land (43%), Sm¯land and Blekinge (26.9%) and Dalarna (12.9%; Fig. 7). The per cent age of rocks from Uppland is very low (6.4%).
This in di cates that the ice sheet was sup plied with rock ma te rial which orig i nated mostly from south-west ern Fennoscandia. This con clu sion is sup ported by the low per cent age of car bon ate rocks (15.51%) and the com - plete ab sence of dolomites in the Fennoscandian rock group. The high con tent of clastic rocks (as much as 18.97%) is an ad di tional in di ca tor of this “west ern”
source area be cause most of the Lower Pa leo zoic sand stone out crops oc cur in the west ern part of the Bal - tic De pres sion and in Swe den.
The The o ret i cal Boul der Cen tre for the till in the site stud ied has the geo graph ical co or di nates 18.29°E and 59.13°N. It is sim i lar to that cal cu lated for the lower basal tills oc cur ring in cen tral-east ern Po land (Czubla et al., 2010a, b). This po si tion of the TBC is char ac ter is tic for the till of the San 2/Elsterian Gla ci ation, i.e. Ma rine Iso tope Stage MIS 12 (see Fig. 1).
PALAEOBOTANICAL ANALYSIS
The re sults of pol len and plant macrofossil anal y ses are shown to gether. Pol len spec tra in form mostly about ter res trial veg e ta tion at lo cal and re gional scales, while plant macrofossils serve as the ba sis for re con struct ing lake veg e ta tion, and in di rectly also in form about the lake trophic lev els.
The pol len spec tra be long to 5 lo cal pol len as sem - blage zones (LPAZs; Fig. 8), and spec tra of plant macrofossils to 5 lo cal macrofossil as sem blage zones (LMAZs; Fig. 9). LPAZs and LMAZs were des ig nated with SO1 ab bre vi a tion and num bered from the base up - wards. The low er most sam ples of the suc ces sion in ves - ti gated (from a depth of 310–365 cm) con tained only spo radic sporomorphs so these were not shown in the pol len di a gram. They con tained macrofossils of dwarf birch (SO1-1 LMAZ – Betula nana, sam ples from 314–321 cm depth). The cor re la tion of LPAZs and L MAZs is given in Ta ble 4.
SO1-1 Betula–Juniperus–Betula nana LPAZ (sam - ples from 286–307 cm depth) is char ac ter ized by the pre dom i nance of Betula undiff. pol len (60–68%), grad u - ally in creas ing pol len val ues of Pinus sylvestris t. (up to 15% in the up per sam ple of the zone), the oc cur rence of Picea, and spo radic pol len grains of Larix, Ulmus and Quercus. Among shrubs the pol len val ues of Juniperus are very high (up to 13.5%), while Salix pol len is fre - quent. The con tin u ous per cent age curve of Betula
ainoloK eht morf mar g aid ne lloP .8 .giFakswezsamoD)1OS elo herob(
How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland 245
.9 .giFlissoforcaMainoloK eht morf mar g aid akswezsamoD)1OS elo herob(
nana t. (up to 7.5%) and high fre quen cies of Poaceae and Cyperaceae (up to 6.5%) at tract at ten tion. The zone re flects the de vel op ment of bo real, open birch for ests at the be gin ning of the inter gla cial and is cor re lated with the SO1-2 LMAZ (Ranunculus sceleratus–Urtica dioica–Carex rostrata; sam ples from 290–305 cm depth). Macrofossils of Betula nana and B.
humilis (fruits) in di cate a cool cli mate. At first the catch ment was over grown by veg e ta tion to a small ex tent, which fa voured solifluction pro cesses (many Cenococcum geophillum sclerotia). Salix (rep re sented by boxes) grew on the shores of the lake, as well as plants typ i cal of eutrophic al der carr hab i - tats, i.e. Urtica dioica, Ranunculus sceleratus, Potentilla repens and Stellaria nemorum. The rush belt was formed by Carex rostrata and Typha (tegmens). The pres ence of Potamogeton filiformis (endocarps) in phytocoenoses in di cates that the lake wa ter was cool and mesotrophic (Kolstrup, 1979; Matusz - kiewicz, 2001; Vielichkevich and Zas tawniak, 2006). It was also very trans par ent, and con tained CaCO3 (Bennike et al., 1994), as also in di cated by the oc cur rence of nu mer ous statoblasts of Cristatella mucedo (kland and kland, 2000).
SO1-2 Pinus–Betula–Larix LPAZ (sam ples from 225–278 cm depth), with sim i lar val ues of Pinus sylvestris t. (up to 40%) and Betula undiff. (up to 41%) and a con tin u ous per cent age curve of Larix, rep re sents the trans for ma tion of birch for ests into pine-birch for ests with larch. The veg e ta tion of open ar eas was still wide spread. This zone is cor re lated with the SO1-3 Carex rostrata–Urtica dioica (sam ples from 267.5–283 cm depth) and the older part of the SO1-4 Carex rostrata–Urtica dioica–Ranunculus sceleratus –Nuphar L MAZs (sam ples from 222.5–258.5 cm depth). Veg e ta tion grow ing on the lake shore and form ing the rush belt be came im pov er ished due to a rise in wa ter level, as in di cated by the pre served re mains (ephippia) of Daph nia sp. These in di cate that the lake was deep, with quite cool wa ter and a low trophic level (Szeroczyñska and Zawisza, 2011).
SO1-3 Picea–Alnus–Fraxinus–/Ulmus/ LPAZ (sam ples from 160–215 cm depth). Up wards in the zone the pol len val - ues of Pinus, Betula and Larix grad u ally de crease, those of Picea, Alnus, Fraxinus and Ulmus in crease, and con tin u ous per cent age curves of Quercus, Taxus, Tilia and Corylus ap - pear. The fre quen cies of Cyperaceae also in crease con sid er - ably, and con tin u ous curves of Ar te mi sia and Humulus ap pear.
Spores of Filicales monolete are fre quent.
This zone rep re sents the be gin ning of the for ma tion of wet com mu ni ties of al der carr type with spruce, and ash-al der riverine for ests, prob a bly with oak (?Quercus robur). The lat ter spe cies could have en tered pine com mu ni ties form ing mixed
pine-oak for ests. The zone is cor re lated with the youn ger part of the SO1-4 LMAZ (sam ples from 172.5–212.5 cm depth). The re mains of Urtica dioica and Stellaria nemorum in di cate that these were abun dant in the herb layer of the al der carr for ests.
Ranunculus sceleratus and Rumex maritimus grew on the ex - posed, muddy, pe ri od i cally flooded shores. The re mains of Carduus crispus (fruits) in di cate that this prob a bly grew in wet places. The sun-ex posed slopes were the hab i tat for xe ro phyt ic Fragaria vesca (seeds), Dianthus arenarius (seeds) and Potentilla heptaphylla (seeds). The rush belt was again the hab - i tat of many abun dantly grow ing spe cies. The pre dom i nant Carex rostrata formed high sedge rush. It was ac com pa nied by Typha, Schoenoplectus lacustris, Sparganium emersum, S. microcarpum and Hippuris vulgaris. A con sid er able shallowing of the lake is in di cated by the de vel op ment of Nymphaeaceae, the main rep re sen ta tive of which was Nuphar lutea (seeds). Potamogeton natans and P. dorofeevi (endocarps) as well as Ceratophyllum demersum (fruits) occured among sub merged hy dro phytes. The last of these oc - curs in eutrophic, stag nant or slowly flow ing wa ter, and is in tol - er ant of con sid er able de creases in wa ter level and of dry ing.
How ever, the lake was meso/eutrophic as in di cated by the oc - cur rence of Najas flexilis with an eco log i cal op ti mum in mesotrophic wa ter.
SO1-4 Taxus–Quercus–Abies–/Carpinus/ LPAZ (sam ples from 130–155 cm depth) is char ac ter ized by an in crease in the pol len val ues of Picea up to 17%, Alnus up to 19%, Taxus up to 2% and Corylus up to 2.5%, de creas ing fre quen cies of Betula undiff. to 2%, and val ues of Pinus sylvestris t. rang ing from 31 to 50%. In the up per part of the zone the ap pear ance of con tin u - ous pol len curves of Abies and Carpinus with max ima of 13 and 5%, re spec tively, and the oc cur rence of pol len of thermophilous plants (Pterocarya, Buxus, Hedera, Ilex, Ligustrum, Vitis, Viscum) is no ta ble. Dif fer ent taxa of the Ericaceae fam ily are abun dant among dwarf shrubs, and Salvina natans oc curs among wa ter plants.
The zone rep re sents for est com mu ni ties of the be gin ning of the Mazovian (=Holsteinian) Inter gla cial op ti mum. These were wet for ests of dif fer ent types (ri par ian for ests, spruce for ests with al der, al der carr for ests with yew), fir for ests, and dry-soil for ests with horn beam, oak, ma ple and lime. Thermophilous shrubs and climb ers oc curred in these for ests. The zone is cor - re lated with the SO1-5 LMAZ Sal vin ia natans–Az ol la filiculoides (sam ples from 132.5–162.5 cm depth). The oc cur rence of these two spe cies of thermophilous wa ter ferns, typ i cal of shal - low, warm lakes of the Mid dle Pleis to cene, in di cates a low er ing of wa ter level. The de vel op ment of rush was hin dered. Only Lo cal pol len as sem blage zones Depth
[cm] Lo cal macrofossil as sem blage zones
SO1-5 Pinus LPAZ 105–128
SO1-5 LMAZ Sal vin ia natans–Az ol la filiculoides LMAZ SO1-4 Taxus–Quercus–Abies–/Carpinus/
LPAZ 128–158
SO1-3 Picea–Alnus–Fraxinus–/Ulmus/ LPAZ 158–220 SO1-4 Carex rostrata–Urtica dioica–Ranunculus sceleratus–Nuphar LMAZ
SO1-2 Pinus–Betula–Larix LPAZ 220–283
SO1-3 Carex rostrata–Urtica dioica LMAZ
SO1-1 Betula–Juniperus–Betula nana LPAZ 286–307 SO1-2 Ranunculus sceleratus–Urtica dioica–Carex rostrata LMAZ
Spo radic sporomorphs only 307–365 SO1-1 Betula nana LMAZ
T a b l e 4 Cor re la tion of pol len and macrofossil zones in the SO1 pro file
reeds with Typha could have sur vived be cause dense mats of fern cov ered the sur face of the ox bow lake. The de vel op ment of macrophytes was hin dered, among oth ers of Nymphaeaceae, which com pletely dis ap peared.
SO1-5 Pinus LPAZ (sam ples from 105–125 cm depth) is char ac ter ized by a lower fre quency of sporomorphs, which are mostly de graded, es pe cially in the two top sam ples. Among AP Pinus sylvestris t. is pre dom i nant (54–66%), the val ues of Betula undiff. slightly in crease (up to 10%). Abies (up to 3%), Picea (up to 7%), Alnus (up to 3%) and Carpinus (up to 1%) have con tin u ous curves. Pol len of Ulmus, Fraxinus, Quercus and Taxus ap pear only spo rad i cally. The val ues of Cyperaceae, Poaceae, Ar te mi sia and Rumex acetosa are again slightly higher. The oc cur rence of Comarum palustre, Scheuchzeria palustris and Drosera rotundifolia, as well as the de creas ing spore val ues of Filicales monolete sug gests the de - vel op ment of a mire. Among plant macrofossils only tegmens of Typha sp. are found (sam ple from 112.5 cm depth).
This zone re flects fur ther dom i na tion by pine for ests in the study area. The grad u ally in creas ing de gree of de struc tion of sporomorphs and their de creas ing fre quency, as well as the change of the de posit into a min eral-or ganic one, in di cate that a hi a tus co in cided with the youn ger part of the cli mate op ti mum.
The suc ces sion de scribed, i.e. bo real birch for ests (SO1-1 LPAZ) and birch-pine for ests with larch (SO1-2 LPAZ), which de - vel oped at the be gin ning of the inter gla cial, fol lowed by al - der-spruce com mu ni ties with grad u ally ap pear ing el e ments rep - re sent ing warmer cli mate (ash, elm, oak – SO1-3 LPAZ), and then with yew, fir, horn beam, lime, ma ple and ha zel (SO1-4 LPAZ), is typ i cal of the older part of the Mazovian Inter gla cial.
The lat ter zone con tains sev eral thermophilous plant el e ments in di cat ing a warm and wet cli mate. These are, among oth ers, climb ers (Hedera, Humulus and Vitis), shrubs (Buxus, Ligustrum, Ilex and Viscum) and wa ter ferns (Sal vin ia natans and Az ol la filiculoides). Si mul ta neously oc cur ring high val ues of fir and horn beam, typ i cal of the Mazovian op ti mum (Mamakowa,
2003), are not re corded in the pol len di a gram. How ever, a very good cor re la tion is found with the pol len di a gram of the Mazovian suc ces sion from the nearby Domaszki site (cf. Pidek et al., 2011) re flect ing the de vel op ment of com mu ni ties dom i nated by Carpinus and Abies. This ad di tion ally sup ports the Mazovian age of the suc ces sion in ves ti gated. A dis tinct sign of its Mid dle Pleis - to cene age is also the oc cur rence of Pterocarya and Az ol la, which did not oc cur in the Eemian and the Ho lo cene. The pat tern of veg e ta tion de vel op ment in the lake is also sim i lar to that re - corded in the plant macrofossils of lakes else where in cen - tral-east ern Po land dur ing the Mazovian Inter gla cial (cf., among oth ers, Hrynowiecka and Szymczyk, 2011).
LUMINESCENCE DATING
The equiv a lent dose and sam ple age val ues ob tained us ing the TL method are shown in Ta ble 5, and those ob tained us ing the IRSL method are in Ta ble 6. Ac cord ing to Li and Li (2011), in the MET-pIRIR pro ce dure the de posit age should be de ter - mined us ing the av er age ED value (cal cu lated ED val ues for 250°C and 300°C). The IRSLMET age shown in Ta ble 4 was cal - cu lated in this way.
The lu mi nes cence dates of the point bar de pos its form two dis tinct groups.
The youn ger dates of the point bar de pos its were ob tained by IRSL meth ods (MET-pIRIR: 303 ± 19 ka and 338 ± 21 ka, and pIRIR290: 352 ± 33ka and 364 ± 33 ka). These re sults are out side the range of ap pli ca bil ity of these meth ods, which is de - ter mined at 300 ka be cause the higher val ues are un der es ti - mated in re la tion to the ex pected age (e.g., Yi et al., 2012).
There fore, the dat ing re sults ob tained for the point bars us ing the IRSL meth ods are un der es ti mated.
The older dates of the point bar de pos its were ob tained us - ing TL meth ods (TLMAX: 412–445 ka and TLINT: 408–631 ka).
The age ob tained by these meth ods may be over es ti mated due to short trans port of the sed i ment be fore its de po si tion. Short How to resolve Pleistocene stratigraphic problems by different methods? A case study from eastern Poland 247
Sam ple Depth [m]
Pla teau test [°C]
Max. TL curve [°C]
Equiv a lent dose EDMAX
[Gy]
TLMAX age [ka]
Equiv a lent dose EDINT
[Gy]
TLINT age [ka]
SPB-1 SPB-2 SPB-3 SPB-4 SPB-5 SPB-6
1.4 3.4 2.4 3.2 3.4 2.0
276–295 239–290 262–282 273–295 284–313 276–290
281 282 279 279 287 279
1106 ± 197 1198 ± 123 806 ± 121 1256 ± 177 1509 ± 226 422 ± 65
444 ± 80 431 ± 45 424 ± 64 433 ± 61 445 ± 67 412 ± 63
1283 ± 294 1134 ± 151 1190 ± 245 1183 ± 197 2138 ± 191 532 ± 90
515 ± 118 408 ± 57 626 ± 134
408 ± 69 631 ± 76 522 ± 99
T a b l e 5 The equiv a lent doses and TL ages of the de pos its de ter mined by two means
pIRIR290 MET-pIRIR
Pro file Depth [m]
Equiv a lent dose EDpIRIR290
[Gy]
IRSLpIRIR290 age [ka]
Equiv a lent dose EDMET-pIRIR250
[Gy]
Equiv a lent dose EDMET-pIRIR300
[Gy]
Equiv a lent dose EDMET-pIRIRmid
[Gy]
IRSLMET-pIRIRmid
age [ka]
SPB-1 SPB-2
1.4 3.4
877 ± 70 1013 ± 76
352 ± 33 364 ± 33
785 ± 53 914 ± 57
726 ± 55 968 ± 61
755 ± 30 941 ± 27
303 ± 19 338 ± 21 Re cy cling ra tio
SPB-1 SPB-2
1.4 3.4
1.00 ± 0.01 1.04 ± 0.01
1.01 ± 0.01 1.01 ± 0.01
0.96 ± 0.01 0.99 ± 0.01
T a b l e 6 The equiv a lent dose and de posit age val ues de ter mined us ing the pIRIR290 and MET-pIRIR pro ce dures
sed i ment trans port hin ders to tal bleach ing of the de pos its (£anczont et al., 2013). Such a sit u a tion can be ex cluded in the case of point bars be cause chan nel de pos its are formed in the mid dle and lower reaches of river val leys, i.e. a long dis tance from the source area. How ever, the wide time span of their de - po si tion as in di cated by the TLINT method is not plau si ble. This would in clude the pe riod from MIS 13 to MIS 11, that is, two inter gla cial pe ri ods sep a rated by a gla cial (Fig. 1). In this case the me an der ing river pat tern should have been trans formed into a braided one dur ing the gla cial cor re lated with MIS 12; this is not re corded in the de pos its in ves ti gated. There fore, the most prob a ble age of the point bar is given by the TLMAX
method: 412–445 ka. This age cor re sponds to the fi nal phase of the Sanian 2/Elsterian Gla ci ation and the be gin ning of the Mazovian (=Holsteinian) Inter gla cial (MIS 12-11; Fig. 1). The re sults of thermoluminescence dat ing in di cate that the TLMAX
method is the most re li able in the as sess ment of the sec tion stud ied.
Sim i lar TL re sults (approx. 430 ka) have been ob tained for silty sands un der ly ing or ganic-clastic de pos its of Mazovian/Holsteinian age in east ern Po land (Nitychoruk et al., 2005). These dates cor re spond to the end of the Sanian 2/Elsterian Gla ci ation (MIS 12; Fig. 1).
SUMMARY OF RESULTS AND CONCLUSIONS
Two waterlain Pleis to cene suc ces sions of dif fer ent or i gin have been iden ti fied by de tailed sedimentological anal y sis of the pres ent-day Samica val ley infill: glaciofluvial unit B and flu - vial unit C. These de pos its are char ac ter ized by dis tinct tex tural and struc tural fea tures. Glaciofluvial unit B, con tain ing channelized fa cies, re flects a braided flu vial sys tem typ i cal of se vere cold cli mate. By con trast, the youn ger unit C com posed of point-bar (sub unit C-1) and ox bow fa cies (sub unit C-2) was de pos ited in a me an der ing river, a flu vial en vi ron ment char ac - ter is tic of a tem per ate cli mate. More over, these flu vial sys tems flowed in op po site di rec tions: the glaciofluvial wa ter flowed south wards, and the me an der ing river to the north.
The strati graphic po si tion of flu vial unit C was de ter mined by means of palaeobotanical anal y ses of ox bow lake de pos its (sub unit C-2) as well as in di rectly by petrographic anal y sis of the till (unit A) in which the flu vial de pos its are in cised. Lu mi nes - cence dat ing of point-bar de pos its (sub unit C-1) was car ried out to es ti mate the age of flu vial unit C. Our find ings lead to the fol - low ing strati graphic con clu sions:
1. Petrographic anal y sis in di cates that the basal till of the till plain con tains in di ca tor er rat ics typ i cal of south-west ern Fennoscandia. The The o ret i cal Boul der Cen tre (TBC: 18.29°E and 59.13°N) is sim i lar to that cal cu lated for tills of the San 2/Elsterian Gla ci ation (MIS 12) in cen tral-east ern Po land.
Thus, the for ma tion of the Samica River fos sil val ley started af - ter this ice-sheet re treat.
2. Based on palaeobotanical anal y ses of the ox bow de pos - its, the suc ces sion was di vided into five lo cal pol len zones (LPAZs) and five lo cal macrofossil zones (LMAZs). The first
four L PAZs, cor re lated with the LMAZs, are typ i cal of the older part of the Mazovian (=Holsteinian) Inter gla cial. They rep re sent the fol low ing suc ces sive phases of veg e ta tion de vel op ment:
– open birch for est at the be gin ning of the inter gla cial. A shal low lake with poor lakeshore veg e ta tion, and cool and mesotrophic lake wa ter;
– birch-pine for est. A rise in wa ter level in the lake and im - pov er ish ment of the lakeshore veg e ta tion com po si tion.
The lake wa ter was still cool and weakly mesotrophic.
– Wet for est of al der carr type, and ash-al der riverine for - est. The shallowing lake was sur rounded by a wide belt of high sedge rush. The lake wa ter was warm, meso/eutrophic;
– thermophilous and hygrophilous for est com mu ni ties around the lake, in clud ing a riverine for est with Pterocarya dur ing the cli ma tic op ti mum of the inter gla - cial. The still shallowing lake was over grown by wa ter ferns – Sal vin ia natans and Az ol la filiculoides.
3. The lu mi nes cence ages of the point bar de pos its form two dis tinct groups:
– youn ger ages were ob tained by IRSL meth ods (MET-pIRIR: 303 ± 19 ka and 338 ± 21 ka, and pIRIR290: 352 ± 33ka and 364 ± 33 ka). The re sults are out side the range of ap pli ca bil ity of these meth ods (300 ka), and so are un der es ti mated;
– older ages were ob tained by TL meth ods (TLMAX: 412–445 ka and TLINT: 408–631 ka). As the de po si tion of the point bar de pos its was con tin u ous, we have to ex - clude the broad time span ob tained by the TLINT method.
The most prob a ble age of these de pos its is in di cated by the re sults from the TLMAX method: 412–445 ka. These cor re spond to the end of the San 2/Elsterian Gla ci ation and the be gin ning of Mazovian/Holsteinian Inter gla cial (MIS 12-11).
The re sults ob tained us ing the three dif fer ent meth ods are com pat i ble, and in di cate that the al lu vial de pos its un der study were formed in a river chan nel and ox bow lake from the end of Elsterian to the op ti mum of the Mazovian (=Holsteinian) Inter - gla cial. These are the first Holsteinian flu vial de pos its to be stud ied sedimentologically in Po land and in deed in Cen tral Eu - rope.
Other strati graphi cal meth ods use fully com ple mented the palaeobotanical anal y ses. Lithofacies anal y sis en abled rec og - ni tion of me an der ing river de pos its typ i cal of warm cli ma tic con - di tions. Petrographic anal y sis of grav els larger than 20 mm, still rare as a tech nique, al lowed as sig na tion of till lev els to par tic u - lar gla cial pe ri ods. The use of the TLMAX method in dat ing de - pos its older than 400 ka has been con firmed.
Ac knowl edge ments. This work has been fi nan cially sup - ported by the Pol ish Min is try of Sci ence and Higher Ed u ca tion pro ject no. N N306 198739 “Cli ma tic cy cles of Mid dle Pleis to - cene re corded in sed i men tary suc ces sion in the £uków re gion (E Po land)”. The valu able com ments of P. Gibbard and an anon y mous re viewer were of great help in im prov ing the manu - script.
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