The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land)
Jan DZIER¯EK1, *, Leszek LINDNER1 and Jerzy NAWROCKI2, 3
1 Uni ver sity of War saw, In sti tute of Ge ol ogy, ¯wirki i Wigury 93, 02-089 Warszawa, Po land
2 Maria Cu rie-Sk³odowska Uni ver sity, Fac ulty of Earth Sci ences and Spa tial Man age ment, Al. Kraœnicka, 2cd, 20-031 Lublin, Po land
3 Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land
Dzier¿ek, J., Lindner, L., Nawrocki, J., 2020. The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land). Geo log i cal Quar terly, 64 (2): 252–262, doi: 10.7306/gq.1527
As so ci ate Ed i tor: Wojciech Granoszewski
The W¹chock sec tion (N part of the Holy Cross Moun tains) is bi par tite, with a sub-loess lower part and a loess up per part.
The sub-loess part ly ing on Lower Tri as sic sand stones in cludes flu vial, gla cial and ice-dammed lake de pos its, TL-dated at 352 ky BP to 157 ±23 ky BP. They rep re sent the Mazovian (MIS 11) (Zbójnian?, MIS 9?) Inter gla cial and the Odranian Gla ci - ation (MIS 6). The up per part com prises loesses in ter ca lated with palaeosols, which reach a to tal thick ness of 9 m and have TL ages at 148 ±23 ky BP to 15.8 ±8 ky BP. This part of the suc ces sion be gins with ho ri zon B of a brown soil from the Eemian Inter gla cial (MIS 5e) with an interstadial black soil from the old est Vistulian (MIS 5c). Four youn ger loess ho ri zons from the mid dle and youn ger Vistulian oc cur above; loesses with arc tic and tun dra palaeosols cor re spond to youn ger iso tope stages (MIS 5b–MIS 2). The loess and palaeosol ho ri zons dis tin guished in W¹chock were cor re lated with loess sec tions in Po land (Zwierzyniec and Polanów Samborzecki) and west ern Ukraine (Kolodiiv 3), show ing large sim i lar i ties of both loesses and palaeosols. Due to this, the W¹chock site is pro posed as a one of key sec tions for Vistulian loess se quences not only in the Holy Cross Mts. re gion but also in Cen tral Eu rope. Palaeomagnetic stud ies of the W¹chock loesses have reg is tered palaeomagnetic in cli na tions with val ues lower than the av er age val ues ex pected in this lo cal ity (63°).
Key words: East-Cen tral Eu rope, loess stra tig ra phy, soil com plexes, TL-dat ing, palaeomagnetism.
INTRODUCTION
Among ter res trial de pos its, loess is of great im por tance for palaeo geo graphi cal stud ies, be ing a car rier of rich palaeo - climatic and palaeoenvironmental data, which of ten cover the whole Pleis to cene. The ba sic re cord of palaeoenvironmental changes is re flected in loess-palaeosoil se quences noted in ex - po sures (Kemp, 2001; Jary, 2007). Dust ac cu mu la tion took place in a cold and dry cli mate (gla cial, stadial), whereas soils de vel oped un der warm and hu mid cli ma tic con di tions (inter gla - cial, interstadial; Jahn, 1950). Based on multi-proxy stud ies of loess-palaeosoil se quences, de tailed strati graphic schemes were pro posed and suc cess fully cor re lated with the deep-sea core data (e.g., Kukla, 1977; Maruszczak, 1991, 2001; Jary, 2007; £anczont and Bogutsky, 2007). Loess pro files also store data on the in ten sity of ac cu mu la tion pro cesses (Fedorowicz
and £anczont, 2007), con di tions of soil de vel op ment (£anczont and Bogutsky, 2007; £¹cka et al., 2007; Nawrocki et al., 2007), wind di rec tion and source of the ma te rial (Chlebowski and Lindner, 1975, 1992; Racinowski, 2007; Bradák et al. 2018), as well as on the de vel op ment of per ma frost pro cesses (Jersak, 1975; Chlebowski and Lindner, 1989; Jary, 2009) and oth ers.
Due to its lo ca tion in the north ern zone of loess oc cur rence in Eu rope and the long his tory of re search, the W¹chock site is an im por tant point in the dis cus sion on ae olian de po si tion in the re - gion, es pe cially af ter con sid er ing the novel data pre sented in this study. Es pe cially im por tant is the fact that stud ied loess de - vel oped on gla cial de pos its of a pen ul ti mate gla cial cy cle and ap pears to con tain the full re cord of cli ma tic changes of the Up - per Pleis to cene.
The main aim of the study is the re con struc tion of the pat - terns of cli mate change in the last inter gla cial-gla cial cy cle based on de tailed in ves ti ga tion of loess and palaeosoils. It also fo cuses on the ver i fi ca tion of pre vi ous re sults and their cor re la - tion with loess pro files of south ern Po land and west ern Ukraine.
We show that the W¹chock pro file is unique due to the abun - dance of re corded palaeoenvironmental changes and thus may of fer a cor re la tion bench mark and a source of better knowl edge of cen tral Po land palaeo ge ogra phy in the extraglacial area of the last gla ci ation.
* Cor re spond ing au thor, e-mail: j.dzierzek@uw.edu.pl
Re ceived: No vem ber 5, 2019; ac cepted: Jan u ary 24, 2020; first pub lished on line: April 14, 2020
The loess suc ces sion in W¹chock was ana lysed for the first time by Karaszewski (1954), who found a tooth of a mam moth (Elephas primigenius) in the wall of the ra vine in loess ly ing above palaeosol from the last inter gla cial. A de tailed study of Pleis to cene sed i ments oc cur ring there was per formed in the late 1970s (Karaszewski et al., 1977; Lindner and Prószyñski, 1979) and the ob tained re sults, in clud ing TL-dat ing, were cor re - lated with the ar chae o log i cal site at Zwierzyniec (Lindner and Madeyska, 1980). Later, the sec tion was ex posed once again (Boguszewski, 2000), and sam ples for sub se quent TL-dat ing (Kusiak, 1999) and palaeomagnetic anal y ses (Piotrowska, 2007) were col lected. Pre lim i nary re sults of these anal y ses were pre sented dur ing the XXVI Con fer ence Pleis to cene Stra - tig ra phy in Po land (Dzier¿ek et al., 2019b).
GEOLOGICAL SETTING
The ana lysed loess sec tion in W¹chock (north ern part of the Holy Cross Moun tains) is lo cated in a small loess is land, 6 km long and 3 km wide (Fig. 1). This loess be longs to the north ern mar gin of the Eu ro pean loess belt spread ing from Ukraine, through south ern Po land, to West ern Eu rope. The most com - plete sec tion was mea sured in the west ern part of the ra vine.
The ra vine rep re sents a very young landform. Ac cord ing to his - tor i cal data, to wards the end of the 19th cen tury the stream in the ra vine was nar row enough to be crossed by pu pils of the nearby ju nior high school. At pres ent, the ra vine walls are 20–30 m apart and their height ex ceeds 15 m in places (Fig. 2).
MATERIAL AND METHODS
The re search ob jec tives were achieved through de tailed lithological and strati graphi cal char ac ter is tics of ex posed sed i - ments in the W¹chock pro file with re gard to ar chi val data, un - pub lished re sults of TL dat ing, and new palaeomagnetic re - sults. The study in cludes the older, sub-loess part of the sec - tion, rep re sented by gla cial de pos its of the sec ond last gla ci - ation (Lindner, 1978, 1980, 1984), and a youn ger, loess part of the sec tion com pris ing a Vistulian loess-palaeosol suc ces sion.
The up per part of the sec tion was sub ject to grain-size and car - bon ate con tent anal y ses. The pres ence of hu mus and the ob - tained re sults were ana lysed tak ing into ac count pre vi ous stud - ies (see Karaszewski et al., 1977).
A dif fer ent meth od ol ogy was ap plied for de tailed anal y sis of the mid-loess palaeosols from the old est (inter gla cial) for est soil to youn ger (tun dra-type) soils, rep re sent ing interstadials of the Vistulian Gla ci ation. These soils are char ac ter ized by con tem - po rary cli ma tic con di tions and cor re spond well to the ex ist ing veg e ta tion con di tions (Granoszewski, 2003). The loess- palaeo sol part of the suc ces sion was also sub ject to palaeomagnetic anal y sis. The ana lysed loess sec tion was cor - re lated with loess sites of that age from Po land and west ern Ukraine (Lindner and Madeyska, 1980; Jary, 2007; £anczont and Boguckyj, 2007). The loess-soil stra tig ra phy is ac cord ing to Maruszczak (2001). Based on the anal y sis of heavy min eral com po si tion (Chlebowski and Lindner, 1992), the source ar eas for the ma te rial of the Up per Youn ger Loess (LMg) and the di - rec tion of loess-form ing winds were es tab lished. The re sults were cor re lated with re gional palaeoclimatic data for the Late Pleis to cene (Marks et al., 2019).
RESULTS
LITHOLOGY
The old est strata are Lower Tri as sic sand stones (Studencki, 1993), over lain by flu vial gravel and sands with a thick ness of 0.5 m, with clasts of lo cal and Scan di na vian ma te - rial (Fig. 3). The dis tri bu tion of these de pos its and their re la tion to the over ly ing varved-clays, 0.5 m thick, and gla cial till, up to 3.5 m thick, in di cate that they were de pos ited dur ing an in ter val di rectly pre ced ing the ad vance of the Scan di na vian ice sheet of the sec ond-last gla ci ation (Odra – Lindner, 1980, pres ently Odranian – Marks et al., 2016; Lindner and Dzier¿ek, 2019).
The gla cial till is brown-cherry red in col our and has a rel a tively uni form struc ture. In the south ern (higher) part of the ra vine, where Tri as sic sand stones oc cur at rel a tively shal low depths, the till con tains smudges and interbeds of lower Roetian cherry-red clays and thin sand smudges. The interbedding and The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land) 253
Fig. 1. Sketch-map with lo ca tion of the stud ied W¹chock loess sec tion;
lo ca tions of loess sec tions in Zwierzyniec, Polanów Samborzecki and Kolodiiv 3, with which it was cor re lated, are also marked
smudges, as well as the dis tri bu tion of boul ders and rock frag - ments, em pha size the lay ered struc ture of the till. This struc ture seems to be the pri mary prop erty of the gla cial till de rived from the ac tiv ity of the ice sheet in tensely erod ing the rock sub strate.
The grain-size com po si tion of the up per most part of this till is char ac ter ized by an al most 50% con tri bu tion of the sand frac - tion at a rel a tively high con tent (20%) of the clay frac tion (Fig. 3).
The clay frac tion con trib utes up to 30% in the over ly ing silt at a dis tinct de crease of the sand con tent. The sand con tent in the over ly ing layer reaches 90%. Ac cu mu la tion of silt and sand with blocks of lo cal (Tri as sic sand stones) and Scan di na vian ma te rial – de rived from the wash ing out of gla cial till pre served in the higher part of the ra vine – was prob a bly re lated to the re - treat of the Scan di na vian ice sheet of the Odranian Gla ci ation (Lindner, 1978, 1980; Lindner et al., 2016), which ear lier cov - ered the en tire area (cf. Dzier¿ek et al., 2019a). The up per most part of the men tioned sand layer (with a thick ness up to 0.5 m) is char ac ter ized by a higher con tent of the fine frac tion and re - sem bles a sandy cover (of ae olian or i gin?).
These de pos its are over lain by a typ i cal, >9 m thick, loess suc ces sion (Figs. 2–4). From the base (at a depth of 9.2–9.6 m) it be gins with a 40 cm sandy layer af fected by soil pro cesses, prob a bly rep re sent ing ho ri zon B of podzolic soil. The over ly ing dis tinct hu mus ho ri zon rep re sents prob a bly chernozemic soil whose top most part shows traces of solifluction. The thin loess layer sep a rates both these soil ho ri zons (cf. Lindner and Madeyska, 1980). The over ly ing yel low-brown cal car e ous loess (Low est Youn ger Loess – LMn) at tains a thick ness of 1.5 m and con tains traces of two poorly de vel oped ho ri zons of tun dra glayed soil at a depth of 7.8–8.7 m. In the top most part of this loess, at a depth of 6.7–7.0 m, oc curs a well-de vel oped tun - dra soil cov ered with 1.4 m of yel low cal car e ous loess (Lower
Youn ger Loess – LMd). This loess is cov ered with a sub se - quent, well-de vel oped, prob a bly bi par tite tun dra soil, at a depth of 5.4–5.7 m.
At a depth of 4.4–5.4 m, there is the non-cal car e ous yel low Mid dle Youn ger Loess (LMs), on which an up per soil com plex is de vel oped. It com prises three over lap ping soil ho ri zons, em - pha sized by iron pre cip i ta tions. They are pre served at a depth of 3.6–4.4 m and reach a to tal thick ness up to 0.8 m. All these ho ri zons are in cised by a 1 m long ice wedge, filled with the cal - car e ous yel low Up per Youn ger Loess (LMg). The youn gest loess layer is al most 2.5 m thick. No breaks in ae olian ac cu mu - la tion of this ma te rial were noted in this loess; in turn, its up per part is char ac ter ized by in creased con tent of gar nets, zir cons, am phi boles and epidotes, which are ob served also in its lower part (see Karaszewski et al., 1977). This fact, cou pled with the upsection-in creas ing sand con tent and the oc cur rence of sand smudges, points to the close vi cin ity and si mul ta neous blow ing out of gla cial sed i ments and waste-man tle of Tri as sic sand - stones, and ae olian in cor po ra tion of this ma te rial into the W¹chock loess mass.
PALAEOSOLS
Palaeosol ho ri zons char ac ter iz ing the up per, loess part of the W¹chock sec tion are rep re sented by two main soil com - plexes, oc cur ring in the lower (depth 8.7–9.6 m) and up per (depth 3.6–4.4 m) parts of the sec tion, and four ini tial gley ho ri - zons oc cur ring within the loess sep a rat ing the two main com - plexes (Fig. 4).
The lower soil com plex (Fig. 5A) is re ferred to in Po land as the “Nietulsko I soil com plex” (Jersak, 1965, 1973) and marked as Gi + GJ1 (Maruszczak, 1991, 2001; Jary, 2007). The (illuvial) ho ri zon B within this com plex is the low er most, leached part of a Fig. 2. West ern side of the loess ra vine in W¹chock. Loesses of the Vistulian Gla ci ation oc cur in the up per part
of the ra vine wall, and the gla cial till from the Odranian Gla ci ation oc curs in the lower part of the ra vine wall
for est (podzolic) soil com monly linked with the Eemian Inter gla - cial (GJ1). Soil de vel op ment at that time was fa voured by a warm cli mate with con sid er able oce anic in flu ence (Marks et al., 2019) and dom i nance of for ests with Quercus and Corylus in the inter gla cial op ti mum (Œrodoñ and Go³¹bowa, 1956;
Jastrzêbska-Mame³ka, 1985). An im por tant part of this com plex is chernozemic, over lap ping the ear lier de pos ited loess, whose ac cu mu la tion was the con se quence of trends of cli mate aridification and cool ing from the end of the Eemian Inter gla cial (Kaliñska-Nartiša et al., 2016; Marks et al., 2019). This chernozemic soil is cor re lated (Jersak, 1973; Maruszczak, 1991; Jary, 2007) with the Brörup Interstadial (Gi/GJ1), which in the pol len sec tions of cen tral Po land is re corded as the first warm for est sta dium of the Vistulian (Mamakowa, 1989). A suc - ces sive cli mate change in the Early Vistulian (Weichselian) re - sulted in the ac cu mu la tion of a se quence of min eral and or ganic de pos its with a re cord of de for es ta tion and ex pan sion of tun dra veg e ta tion in nu mer ous sec tions of cen tral Po land (Jastrzêbska-Mame³ka, 1985; Granoszewski, 2003; Kaliñska- Nartiša et al., 2016; Marks et al., 2019). The above-pre served Low est Youn ger Loess (LMn) con tains two poorly de vel oped
ho ri zons of gley tun dra soils in the lower part (Fig. 4). The de - vel op ment of these loesses could char ac ter ize short breaks in ac cu mu la tion at the bound ary be tween tun dra and arc tic cli - mates. The well-de vel oped tun dra soil in the top most part of the Low est Youn ger Loess (Fig. 5B) can in di cate the cli ma tic con di - tions as typ i cal for the older interstadial (Gi/LMn = Odderade).
The sub se quent gley ho ri zon, pre served in the top most part of the Lower Youn ger Loess (LMd), is char ac ter ized by a greater thick ness and a bi par tite struc ture (Fig. 5C). The de vel - op ment of this soil pro file can be re lated to the Oerel (lower ho ri - zon) and Glinde (up per ho ri zon) Interstadials, when sub arc tic cli mate pre vailed in the area of Po land (Granoszewski, 2003;
Marks et al., 2019).
The up per soil ho ri zon (Figs. 4 and 5D) is pre served above the Mid dle Youn ger Loess (LMs); in cen tral Po land it is re ferred to as the “Komorniki soil” (Jersak, 1965, 1973). In the W¹chock sec tion, it is de vel oped as three ac cu mu la tion-gley ho ri zons, poorly ex pressed by illuvial ho ri zons. The com plex is char ac ter - ized by a rel a tively high or ganic car bon con tent and a higher con - tent of col loi dal parts com pared to the over- and un der ly ing loesses. Strong decalcification be low this ho ri zon is sur pris ing.
The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land) 255
Fig. 3. Lithological col umn of the W¹chock sec tion
It may be linked with short but over lap ping gley pro cesses (Fig. 5D). Ac cord ing to ear lier sug ges tions (Karaszewski et al., 1977), the up per soil com plex rep re sents the main megainterstadial of the Vistulian (Gi/LMs), en com pass ing three interstadials: Moershoofd, Hengelo and Denekamp. Pol len anal - y sis of the lake-peatland sed i ments from this part of the Vistulian in di cates that a steppe-tun dra with lo cal pres ence of bush tun dra cov ered the area of cen tral Po land at that time (Granoszewski, 2003; Dzier¿ek, 2009; Dzier¿ek and Szymanek, 2013; Marks et al., 2019). In ci sion of the soil by an ice wedge is re lated to in ten si - fi ca tion of pro cesses within the per ma frost in an in ter val pre ced - ing the de vel op ment of the last ice sheet dur ing MIS 2 (e.g., Dzier¿ek and Stañczuk, 2006; Dzier¿ek, 2009; Marks et al., 2016, 2019; Ewertowski et al., 2017).
TL DATING
The ana lysed sec tion was sub ject to TL age de ter mi na tions dur ing three stages (Fig. 4). The first stage in cluded TL dat ing of the en tire sec tion, per formed by M. Prószyñski (Lindner and Prószyñski, 1979) in the lab o ra tory of the Fac ulty of Ge og ra phy and Re gional Stud ies of the Uni ver sity of War saw. The old est age of 352.0 ky BP was ob tained for grav elly-sandy de pos its cov er ing the Tri as sic sand stones. A youn ger age of 245 ±45 ky BP was noted for the basal part of silts cov er ing the gla cial till.
The next age of 142 ±36 ky BP was es tab lished for the over ly ing sands pre served above the silts. The old est age, 42.0 ±1.5 ky BP, was mea sured from the loesses in the lower part of the sec - tion, and two youn ger ages, 24.0 ±2.5 ky BP and 15.8 ±1.8 ky Fig. 4. W¹chock loess sec tion and its age de ter mi na tion
Palaeomagnetic data and mag netic sus cep ti bil ity af ter Piotrowska (2007); ex pla na tions as on Fig ure 3
BP, were at trib uted to the loesses be low and above the up per com plex of megainterstadial soils in cised by the frost wedge (Figs. 3 and 4).
The sec ond stage of TL dat ing was fo cused only on loesses from the stud ied sec tion and was per formed in the same lab o ra - tory as the stage 1 anal y ses (Prószyñska-Bordas, 1983). Two dates were ob tained, of which the older of 43.0 ±6.0 ky BP and the youn ger of 39.0 ±6.0 ky BP cor re sponded to the lower and mid dle part of the sec tion, re spec tively (Fig. 3).
The third stage of TL dat ing was per formed by Kusiak (1999) in the lab o ra tory of the De part ment of Phys i cal Ge og ra - phy and Palaeo ge ogra phy of Maria Cu rie-Sk³odowska Uni ver - sity in Lublin (Ta ble 1).
The ob tained re sults most fully doc u ment the TL ages of the ana lysed loesses and in ter ven ing palaeosols. These re sults
The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land) 257
Depth [m]
Lab. No Lub-
An nual dose Dr [Gy/ka]
Geo log i cal dose ED [Gy]
Age [ky]
5.3 3644 3.284 211 ±29 64 ±9
5.7 3645 3.356 230 ±30 68 ±10
6.9 3646 3.138 226 ±34 72 ±11
7.9 3647 3.526 246 ±37 70 ±11
8.6 3648 3.078 263 ±34 85 ±12
8.9 3649 1.597 236 ±35 148 ±23
9.5 3650 1.602 252 ±35 157 ±23
T a b l e 1 Re sults of TL dat ing for the W¹chock leoss sec tion
(af ter Kusiak, 1999) Fig. 5. Frag ments of the W¹chock loess sec tion
A – GJ1 – ho ri zon B of soil from the Eemian Inter gla cial, Gi/GJ1 – chernozemic soil from the Brörup Interstadial, LMn – Low est Youn ger Loess; B – LMn – Low est Youn ger Loess, Gi/LMn – older interstadial tun - dra soil, LMd – Lower Youn ger Loess; C – LMd – Lower Youn ger Loess; Gi/LMd – bi par tite, youn ger interstadial tun dra soil; D – Gi/LMd – youn ger interstadial tun dra soil, LMs – Mid dle Youn ger Loess, Gi/LMs – youn gest, tri par tite arc tic interstadial soil
largely con firm the strati graphic in ter pre ta tion of the sed i ments per formed on the ba sis of their lithological anal y sis and the ge - netic-cli ma tic char ac ter is tics of the palaeosols (Fig. 4).
The old est age of 157 ±23 ky BP con firms the age for the sands ear lier es tab lished as older from the Eemian Inter gla cial.
The youn ger age of 148 ±23 ky BP also con firms the age of the up per part of the “Nietulisko I soil com plex” (Gi/GJ1), and the three up per dates of 85 ±12 ky BP, 70 ±11 ky BP, and 72 ±11 ky BP con firm the age of the Low est Youn ger Loess (LMn) and the youn ger interstadial (Odderde, Gi/LMn). Two sub se quently youn ger ages of 68 ±10 ky BP and 64 ±9 ky BP, ob tained for the Lower Youn ger Loess (LMd) and Mid dle Youn ger Loess (LMs), re spec tively, in di cate that the palaeosol lo cated be tween them rep re sents the Oerel + Glinde Interstadials (Gi/LMd).
PALAEOMAGNETIC ANALYSIS
Anal y sis of the rem nant geo mag netic field was made dur ing a M.Sc. study (Piotrowska, 2007) for 85 loess sam ples col - lected from the first 8 m of the sec tion (Fig. 4). The sam ples were de mag ne tized in an al ter nat ing mag netic field with an am - pli tude of up to 100 mT. The chart of char ac ter is tic palaeo - magnetic dec li na tions and in cli na tions along the ana lysed sec - tion in di cates that all sam ples re cord a mag netic field with a nor - mal po lar ity. There fore, the sec tion does not con tain sam ples from at least two ex cur sions of the geo mag netic field, which took place in this part of the Pleis to cene at 33 ky BP and 41 ky BP (e.g., Singer, 2014). In the up per part of the sec tion, in cli na - tions ob tained for most sam ples at tain lower val ues com pared to the av er age in cli na tion ex pected in the study lo cal ity (63°).
This fact may point to sed i men ta tion of this part of the suc ces - sion on a slope. This con clu sion seems to be con firmed by the dis tri bu tion of the axis of mag netic ani so tropy mea sured in the up per part of the W¹chock sec tion (Fig. 6). The ev i dent dip of the axis of min i mal sus cep ti bil ity and the axes of max i mal sus -
cep ti bil ity ran domly dis trib uted on the large cir cle may be linked with sed i men ta tion on a slope, ori ented prob a bly to the south (see Nawrocki et al., 2006; Bradák et al., 2018).
Mag netic sus cep ti bil ity val ues for loesses and interstadial palaeosols are sim i lar. Lack of in creased sus cep ti bil ity in zones of interstadial soils, and even a de crease of its value, e.g., in the inter gla cial ho ri zon from a depth of ~8 m is prob a bly the ef fect of gley pro cesses. Worth not ing is that the high est val ues of mag - netic sus cep ti bil ity (up to ~350 ´ 10–6 units SI) oc cur in the youn - gest loess lay ers and the youn gest palaeosol (Fig. 4). Such high sus cep ti bil ity of loess may point to rel a tively high ac cu mu - la tion of mag ne tite, which may be the ef fect of short trans port.
DISCUSSION
CORRELATION WITH SELECTED LOESS SECTIONS ZWIERZYNIEC
The at tempt to cor re late the loesses and palaeosols from the W¹chock sec tion with loesses and palaeosols in the ar - chae o log i cal site at Zwierzyniec (Figs. 1 and 7) was un der taken many years ago ow ing to the very sim i lar suc ces sions of the loesses and the typology of sub-loess and mid-loess palaeosols (Lindner and Madeyska, 1980). The Zwierzyniec (Kra - ków– Zwierzyniec) sec tion has been well known for many tens of years, be ing stud ied, e.g., by Sawicki (1952) and Chmielewski et al. (1977). Sev eral Palaeo lithic cul ture ho ri zons were used to date the suc ces sion (Fig. 7).
In ter vals of loess-palaeosol suc ces sions rep re sent ing the Eemian Inter gla cial and the Brörup Interstadial were dis tin - guished both in W¹chock and Zwierzyniec. In the lat ter site they were TL-dated by W. Stañska-Prószyñska (Lindner and Madeyska, 1980) as youn ger than 318.3–306.86 ky BP and older than 75.9–72.95 ky BP. As sem blages of the Levalluois- Mous terian cul ture also oc cur here in both the in ter val rep re - sent ing the Eemian Inter gla cial and above. In the up per part of the sec tion, de ter mined by the cited au thor as older than 71.7–67.6 ky BP, and in W¹chock de ter mined as the Lower Mid dle Loess (LMd), oc cur (prob a bly re de pos ited) artefacts of the Micoquo-Prondnikian cul ture. Artefacts of the Aurig na cian cul ture were re corded higher up, at the base of the
“Komorniki-type” palaeosol (Gi/LMs), and two as sem blages were noted within this palaeosol: Jerzmanowice and Up per Palaeo lithic, cov ered by the Up per Youn ger Loess (LMg) dated at 31.57–27.28 ky BP (Lindner and Madeyska, 1980; £anczont et al., 2015).
POLANÓW SAMBORZECKI NEAR SANDOMIERZ
The sec tion is lo cated on the south east ern mar gin of the Opatów-Sandomierz loess up land (Fig. 1). Ac cord ing to Jary (2007), the sec tion com prises 13 m of loess sep a rated by palaeosols (Fig. 7). It is char ac ter ized by sev eral ho ri zons of periglacial de for ma tion. The sec tion was TL-dated by S. Fedorowicz, J. Kusiak (Kusiak and £anczont, 2000) and OSL-dated by A. Bluszcz (Jary, 2007). From the base it be gins with the illuvial ho ri zon B (eroded) of for est soil from the Eemian Inter gla cial (GJ1) and an over lap ping hu mus ho ri zon (chernozemic soil) of the low er most Vistulian interstadial soil (Gi). A ho ri zon of the Lower Youn ger Loess (LMd) oc curs above, TL-dated at 89.0 ±9.3 ky (Jary, 2007). The loess is char - ac ter ized by the pres ence of four poorly de vel oped gley ho ri - zons (sg) and is cov ered by a bi par tite interstadial soil (Gi/LMd).
Fig. 6. Spher i cal pro jec tion of the axis of mag netic sus cep ti bil ity of palaeomagnetic sam ples from the W¹chock loess sec tion (af ter Piotrowska, 2007)
The two-part soil re sem bles to some de gree the Gi/LMd bi par - tite soil at trib uted to the Glinde Interstadial, pre served in the W¹chock sec tion (Fig. 7).
Above, there is the Mid dle Youn ger Loess (LMs) with four gley ho ri zons (sg), TL-dated at 37.8 ±4.2 ky BP to 24.4 ±3.0 ky BP, and with OSL ages in the range of 28.6 ±2.1 ky BP to 19.3 ±1.2 ky BP (Jary, 2007). Like in the W¹chock sec tion, a very dis tinct gley ho ri zon from the youn gest interstadial (sg/LMs) is pre served in the top most part of this loess; it is also af fected by periglacial de for ma tion. The youn gest part of the sec tion in Polanów Samborzecki is a 2.5 m thick ho ri zon of the Up per Youn ger Loess (LMg) with sev eral gley smudges (spots), not re corded in the W¹chock sec tion.
KOLODIIV 3 (WESTERN UKRAINE)
The Kolodiiv 3 loess sec tion, like other sec tions of this site, has nu mer ous ref er ences (e.g., £anczont and Bogucky, 2007;
Frankowski et al., 2007; Nawrocki et al., 2007). It is lo cated on the right bank of the Sivka River val ley, the trib u tary of the Dniester River. The suc ces sion be gins with al most 4 m of flu vial de pos its. Above, there is 2 m of lake gyttja from the Eemian (Horohiv) Inter gla cial, cov ered by a loess-soil se ries with a
thick ness of 14 m (Fig. 7). The lake de pos its were TL-dated at 164 ±30 ky BP to 146 ±22 ky BP, and the old est loess sed i - ments – at 164 ±26 ky BP (Kusiak, 2007). The loesses are sep - a rated by three palaeosol ho ri zons, partly dis placed downslope. The up per most soil, youn ger than 95 ±15 ky BP, is re ferred to as the Kolodiiv 1 soil and lo cated within the Odderade Inter stadial, whereas two older soils (Kolodiiv 2 and 3) are con sid ered equiv a lents of the Amersfoort and Brörup interstadials (£anczont and Bogucky, 2007). Fol low ing Maruszczak (1991), the over ly ing loess is re ferred to the Lower Youn ger Loess (LMd). A two-part sub arc tic palaeosol is found above, like the anal o gous soils (Gi/LMd) in the W¹chock and Polanów Samborzecki sec tions. In the Kolodiiv 3 sec tion, it is de ter mined as soil (soils) of the Dubno 2 ho ri zon, and the loess ho ri zon above – as the equiv a lent of the Mid dle Youn ger Loess (LMs) in the cited sec tions from Po land.
Sub se quent (1–5) tun dra palaeosol ho ri zons are de vel oped in the top most part of this loess (LMs) in the Kolodiiv 3 sec tion;
their ev i dently over es ti mated TL age was de ter mined at 115 ±28 ky BP to 76 ±12 ky BP (Kusiak, 2007). They are de ter - mined as the Dubno 1 palaeosols and cor re spond to the youn - gest mid-loess interstadials of the last gla ci ation: Moershoofd, Hengelo and Denekamp (£anczont and Bogucky, 2007) – as in The loess sec tion in W¹chock as the key site of Vistulian loesses and palaeosols in the Holy Cross Moun tains (Po land) 259
Fig. 7. Cor re la tion of loesses and palaeosols from W¹chock, Zwierzyniec (Lindner and Madeyska, 1980), Polanów Samborzecki (Jary, 2007) and Kolodiiv (£anczont and Bogutsky, 2007) sec tions
Let ter sym bols for loess and palaeosols af ter Maruszczak (2001); let ter sym bols for ar chae o log i cal assembages af ter Chmielewski et al.
(1977): LM – Levalluois-Mous terian; MP – Micoquo-Prondnikian; OR – Aurig na cian; GP – Jerzmanowice and Up per Palaeo lithic
the case of soils of the “Komorniki-type” com plex in W¹chock.
The as sem blage of these soils in the Kolodiiv 3 sec tion is cov - ered by the Up per Youn ger Loess (LMg) with two ini tial tun dra soils prob a bly be ing the equiv a lents of gley ho ri zons (sg) in the Polanów Samborzecki sec tion (Fig. 7).
CONDITIONS OF LOESS ACCUMULATION AT W¥CHOCK
As it may be con cluded from the above de scrip tion, de pos its rep re sent ing the loess part of the W¹chock sec tion, along with the cor re la tive strata from sec tions in Ma³opolska and Ukraine, cor re spond largely to the cli mate changes in the Late Pleis to - cene of Po land and Cen tral Eu rope (Granoszewski, 2003; Marks et al., 2019). How ever, the re gional in di vid u al ity of loess ac cu mu - la tion in W¹chock is quite clear. Nu mer ous smudges and interbeddings of sandy ma te rial pre served in the Up per Youn ger Loess (LMg), like in many loesses of that age in the west ern part of the Holy Cross Moun tains (Lindner, 1972a), point to rhyth mic blow ing out of the waste-man tle of lo cal sand stones (Buntsandstein and Li assic) dur ing loess sed i men ta tion. High in - ten sity of the con tem po rary ae olian pro cesses in the west ern and north ern part of the area is con firmed also by the dis tri bu tion of cor ro sion-de fla tion sand stone out li ers in the area (Lindner, 1972b). The out li ers bear traces of the ac tiv ity of west erly winds (Chlebowski and Lindner, 1992), whereas the col lected car to - graphic data in di cate that the main cy cle of ae olian mod i fi ca tion took place dur ing the ter mi nal loess-form ing in ter val.
Stud ies of heavy min eral com po si tion in the youn ger loesses build ing the loess is lands in this part of the Holy Cross Moun tains, in clud ing the Up per Youn ger Loess (LMg) in the W¹chock sec tion (Chlebowski and Lindner, 1992), have in di - cated that the com po si tion of trans par ent heavy min er als is dom i nated by mus co vite, bi o tite, am phi boles, as well as chlorite and gar nets. Weath er ing-re sis tant min er als, such as zir con, rutile, tour ma line, staurolite and dystene, oc cur in very small quan ti ties. The com po si tion of these min er als, par tic u larly the quan ti ta tive pro por tions, are clearly re lated to the base ment com posed of rocks of gla cial or i gin (sands and gla cial tills), con - tain ing frag ments of mag matic rocks or their waste-man tle (Chlebowski and Lindner, 1975).
Based on the pres ence of these min er als and the geomorphological set ting of the loess is lands (Lindner, 1967, 1971), it may rather be as sumed that the trans por ta tion dis - tance of the loess-form ing ma te rial was short, as in di cated by the di rect min eral link of loesses with the lo cal source ar eas.
This points that the main trans por ta tion of ae olian loess ma te - rial took place from the west with lo cal de vi a tions from the north-west (cf. Marks et al., 2019). As a rule, the winds were typ i cal for the lower parts of the at mo sphere (Chlebowski and
Lindner, 1989). Palaeomagnetic stud ies of sam ples col lected from the W¹chock sec tion seem to con firm the hy poth e sis that the up per part of the ana lysed loesses could have ac cu mu lated on a slope, lo cally fac ing to the south (Nawrocki et al., 2006).
CONCLUSIONS
Com pi la tion of ar chi val ma te rial and new re ports, in clud ing re sults of TL-anal y sis and palaeomagnetic stud ies of loesses and palaeosols in the W¹chock sec tion, as well as com par i son with other loess sec tions, al lows draw ing the fol low ing con clu - sions.
1. The en tire W¹chock sec tion, in clud ing loesses and palaeosols within them, as well as de pos its from the Odranian Gla ci ation (MIS 6, ac cord ing to Marks et al., 2016) were TL-dated in three stages, of which the first stage fully doc u - ments the age of de pos its from this gla ci ation and the pre - served for est soil from the Eemian Inter gla cial (MIS 5e), and the youn gest age in di cates the po si tion of youn ger loesses and tun - dra soils from the Vistulian Gla ci ation (MIS 5b-2).
2. Palaeosols and loesses in the W¹chock sec tion rep re - sent a par tic u larly com plete suc ces sion of cli mate changes char ac ter iz ing the Vistulian Gla ci ation, which gives a pos si bil ity of re lat ing them to changes re corded in the se quences of lake de pos its in Po land.
3. Both the ana lysed loesses and the in ter ven ing palaeosols were de picted with sym bols sug gested by Maruszczak (1991, 2001) and com monly used by sci en tists study ing loesses in Po land and west ern Ukraine, which al lowed cor re la tion of the ana lysed se quence with type sec tions (Zwierzyniec, Polanów Samborzecki, Kolodiiv 3) in these ar eas.
4. Anal y sis of the rem nant mag netic field has in di cated that the stud ied suc ces sion re cords only nor mal po lar ity, whereas the dip of max i mal po lar ity and dis persed axes of this sus cep ti - bil ity on the large cir cle may reg is ter sed i men ta tion of the up per part of the loesses on a slope fac ing to the south.
5. The at tempt to de ter mine the ac cu mu la tion con di tions of the Up per Youn ger Loess (LMg) in the analysed sec tion, based on anal y sis of its geomorphological po si tion and com po si tion of heavy min er als, point to a lo cal source of loess ma te rial and a west erly and northwest erly di rec tion of the con tem po rary loess-form ing winds.
Ac knowl edge ments. We sin cerely thank Prof. N. Gera - simenko and the Anon y mous Re viewer for crit i cal and help ful com ments on the manu script. We also thank R. Janiszewski for his help in pre par ing the fig ures.
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