Annales Societatis Geologorum Poloniae (2010), vol. 80: 39–52.

DEVELOPMENT OF A FORE-MOUNTAIN ALLUVIAL FAN OF THE RIVER (SOUTHERN ) DURING THE PLEISTOCENE

Tomasz SA LA MON1 & Antoni WÓJCIK1, 2

1 Depart ment of Earth Sci ences, Uni ver sity of , Bêdzi ñska 60, 41-200 Sosnow iec , Poland, e- mail: tomasz.sa la [email protected] 2 Polish Geologi cal Insti tute, Carpa thi an Branch, Skrzatów 1, 31-560 Kraków, Poland, e-mail : antoni .wojci [email protected]

Sa la mon, T. & Wójcik, A., 2010. De vel op ment of a fore- mountain al lu vial fan of the Olza River (south ern Po land) dur ing the Pleis to cene. An nales So cie ta tis Ge olo go rum Po lo niae, 80: 39–52.

Ab stract: A series of Pleis to cene de posits with dif fer ent li thol ogy is pres ent where the Olza River flows out from the Car pa thian foot hills to the Oœwiêcim Basin. The de posits are mostly composed of grav els forming sev eral series of differ ent ages, which are in terca lated with much finer silts and sands as well as organic silts. A complex of gla cio genic de posits is also found as a thin layer of till, gla cio la cus trine and gla cio flu vial sedi ments. Loess- like de posits oc cur in the top part of the sec tion un der study. Grav els were de posited in the zone of a fore- mountain fan. The co- occurrence of litho logi cally dif fer ent de posits re flects a great vari abil ity of sedi menta tion con di tions, which de pended mostly on cli mate changes. However, the for mation of fan was also con trolled by other fac tors. Neo tec tonic move ments proba bly played an impor tant role in its evo lu tion. In this pa per, we de scribe the suc ces sive stages of fan de vel opment and the fac tors de ter mining this pro cess. The in ter pre ta tion is based on the analy sis of de posits ex posed in the eastern part of the fan, at the Koñczyce site. The fan of the Olza River was built up with al lu via mostly dur ing suc ces sive gla cia tions. It was dis sected to wards the end of each gla cia tion. Dur ing in ter gla cials the fan was only slightly trans formed. A spe cial pe riod of fan de vel op ment oc curred dur ing gla cia tion when the ice sheet ad vanced on the fan sur face. The ag gra da tion of the fan was proba bly stopped due to up lift of the area. Then, aeo lian loess-like de posits started to ac cu mulate on a con sider able part of the fan sur face. Former opin ions about the stra tigra phy of the fan de posits are strongly diver si fied. Precise age of the succes sive series is still diffi cult to estab lish. In the light of contem po rary stud ies, it can not be ex cluded that age of the Olza fan might be younger than pre vi ously suggested.

Key words: fore- mountain al lu vial fan, sedi men tol ogy, Pleis to cene, Koñc zyce sec tion, south ern Po land.

Manu script re ceived 16 September 2009, ac cepted 13 January 2010

IN TRO DUC TION

The de velop m ent of allu vial fans de pends on many fac- 1999; Robustelli et al., 2005). The fans are also com mon tors, which are de ter mined mainly by morphol ogy and geol - under cold cli mati c condi ti ons in the northern part of Eu- ogy of the sub stra tum, cli mate con di tions, veg e ta tion cover, rope (cf. LÝnne & Nemec, 2004). During the Pleis tocene , hydro log i cal regim e, amount and type of weathered mate - allu vial fans were formed abundantl y also in other parts of rial de liv ered to the fan, etc. (cf. Beaty, 1963; Schumm, the conti nent, such as mountai n forelands of Centra l Eu- 1977; Boothroyd & Nummedal, 1978; Heward, 1978; rope, i.e. in the and Carpathian forelands (Ksi¹¿kie- Nilsen, 1985; Rachocki & Church, 1990; DeCelles et al., wicz, 1935; Stupnicka, 1963; Starkel, 1967; Gilot et al., 1991; Stanistreet & Mc Car thy, 1993; Blair & McPherson, 1982; Niedzia³kowska et al., 1985; Niedzia³kowska & 1994; Blair, 1999; Viseras et al., 2003). Apart from high- Szczepanek, 1993, 1994; Krzyszkowski, 1993; Badura et moun tain ar eas, the most fa vour able con di tions for de vel op - al., 2005). Their in ten sive de vel op ment fell es pe cially on ment of al lu vial fans oc cur usu ally in mor pho log i cally di- the glaci ati on peri ods. In this pa per, an attem pt is made to versi fie d areas with sparse vege ta ti on, both in warm and re con struct the Pleis to cene evo lu tion of a rel a tively small cold cli mati c zones. In Europe, the fans are found most fre - fan of the Olza River. This fan was formed in the zone, quently in the Medi ter ranean Sea re gion (cf. Nemec & where the Olza River flows out from the Carpathians Foot- Postma, 1993; Amorosi et al., 1996; Guzzetti et al., 1997; hills to the Oœwiêcim Basin (area of the Carpathian Fore- Sorriso-Valvo et al., 1998; Harvey, 1996; Harvey et al., deep). The re construc tion is based on de tailed sedimentolo- 40 T. SALAMON & A. WÓJCIK

Fig. 1. To pog ra phy of the study area with loca tion of the Koñczyce site

gical anal ysis of sed im ents ex posed at Koñczyce. Sed im en - ring over grav els to the “Great” (Hol stein ian) In ter gla cial, tary suc ces sion com prises sev eral se ries of al lu vial grav els and the overlay ing loess to the Wei chse lian Glacia tion. and sands, lo cally in ter ca lated with much finer silts and In the former stud ies the grav els at the Koñczyce site sands as well as or ganic silts. Al lu vial de pos its are capped were re lated to allu vial deposi ti on in an erosiona l trough with loess cover. A com plex of glaciogenic depos it s is oriente d west-eas t, but they were not attri buted to fan envi - found in the middle part of the studied secti on. ronm ent. The authors found many prem ises to support fan- Although the Koñczyc e site has been known in geologi - origin of the sedi ments in ques tion. Moreover, litho fa cie s cal litera ture for over 25 years and ex am ined by many variati on of these sedim ents indi cat es that the fan de veloped authors (Jersak, 1983; Budek et al., 2004; Drewnik et al., in sev eral stages. Each of them was con trolled by dif fer ent 2004; Wójcik et al., 2004), strati graphic posi ti on of the de- en vi ron mental fac tors. pos its is not agreed by all the re search ers. Accord ing to Jersak (1983), the se ries of gravels and sands oc curring in the lower part of the succes sion was MOR PHO LOG I CAL AND GEO LOG I CAL formed during the Middle Polish Glacia tions (Saalian) – SET TING Odranian or nian, whereas organic depos it s and the overlying loess were accu m ulat ed during the Vis tulian The valley of the Olza River, a right-bank tributar y of (Weichselian) Glacia tion. Based on the result s of palyno - the Odra River, dis sects the western part of the Sile sian Be - logi cal and pa laeo mag netic analy ses, Wójcik et al. (2004) skidy Mountai ns and the Ci eszyn Foot hills, oc curring in assum ed these de posit s to be much older. They relat ed the their foreland (Fig. 1). The Carpa thi an part of the catchm ent upper layer of organic depos it s to the Crom erian II–III In- rises over 1,000 m a.s.l., and relati ve heights in this area are ter glacia l, and loess-li ke depos it s to several younger gla cia - about 400–500 m. The area is com posed of flysch serie s be- tions. They also found the lower m ost layer of organic sedi - longing to the Magura, Fore-Magur a, and Silesia n units. ments and gla cial de pos its, and cor re lated it, re spec tively, to The Ciesz yn Foot hills, built up mostly of Juras sic carbon ate the Cro merian I In ter gla cial, and Nare wian Gla cia tion (Me - rocks and Cre ta ceous sili ci clas tic de pos its, are char ac ter - napian). Drewnik et al. (2004) and Budek et al. (2004) stud- ized by hilly re lief with rela tive heights reach ing 70 m. Hill ied the loess depos it s and suggest ed a differ ent age and sum mits reach 350–400 m a.s.l. The mountai n part of the multi- stage de vel op ment of this se ries. Olza River catchm ent is about 380 km2. A similar suc ces sion of sedi ments in the Czech part of The exam ined de posit s of the Olza River fan oc cur the Olza River valley were de scribed by Macoun et al. where the river leaves the Car pa thian Foothills. This area, (1965), who corre lat ed the serie s of gravels and sands to the called the Koñczyce High plain, is a part of the Car pa thian Sanian (El ste rian) Gla cia tion, the or ganic de pos its oc cur- Foredeep (Fig. 1) filled with the Neogene molas se strata. DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 41

Ta ble 1 LITHOFACIES AND THEIR INTER PRE TA TIO N Lithofacies code sym bols used in text and figures Seven sedi men tary se ries of dif fer ent li thol ogy and ori- Textural symbols gin have been disti nguishe d in the Koñczyc e site (Fig. 2). G gravel GS gravelly sand (1) Lower se ries of grav els The lower se ries of gravels is about 12–15 m thick. SG sandy gravel Only its upper part, of the thickness of about 4–6 m, is visi- S sand ble in ex po sures (Fig. 3A). Li tho fa cies as so cia tion Gm, SF silty sand (GSh, Sm, SGp) is dis tinguishe d in this part of the secti on (Fig. 2). It is dominate d by litho fa cie s of matrix-supporte d FS sandy silt gravels and sandy gravels with massive struc ture Gm (Fig. F silt 3B). The gravel clasts reach 2–6 cm, and rarely exceed D diamicton 10 cm in di ameter . The thickness of li thofa cie s Gm is small or medium (5–30 cm), sporadi cally up to 50 cm. Subor di - Structural symbols nate li tho fa cies of sandy grav els with hori zon tal strati fi ca - m massive structure tion GSh reach the thickness of a dozen or so centi metre s. h horizontal lamination/stratification Gravel beds are spo radi cally inter calated with thin (3– 10 cm), of ten dis con tinu ous li tho fa cies of mas sive sands p tabular cross-stratification Sm. In other places medium-sca le gravell y sands or sandy t trough cross-stratification gravels with planar cross-stra tification SGp or low- angle l low-angle cross-stratification cross-strat i fi ca tion SGl are fre quent li tho fa cies (Fig. 3C). Ice- wedges were ob served in this se ries at sev eral lev els. r ripple cross-lamination They are few deci metres high, a dozen or so cen tim etres wide, and filled with gravelly-sandy sedi ments (Fig. 3D). The de scribed sedi ments rep re sent the en vi ron ment of a very shal low gravel- bed braided river (cf. Williams & Rust, 1969; Smith, 1970; Rust, 1972; Miall , 1977). The sedi ments The stud ied sedi ments di rectly over lie Miocene clays. were de posit ed as thin gravel sheets (the ori gin of thin litho - The de scribed fan is not visible in the present reli ef be- facie s Gm and GSh) or low and flat longi tu di nal bars (the cause it is buried by loess-li ke depos it s, a dozen or so metre s origin of thicker li thofa cie s Gm). The deposi ti on occurred thick. This area is an undu lat ed highland (about 260–280 m during flood peaks from super cri ti cal and transi ti onal flows. a.s.l.) with relati ve heights up to 30 m. The fan prograded Poor sort ing of matrix-supporte d gravels indi cat es that the towards the north. It was a dozen kilom etre s long and up to depo si tion was sud den. Li tho fa cies Sm were also de pos ited 10 km wide. The eleva ti ons com posed of Miocene strata as thin sheets. They were formed during waning flood and rising 270–280 m a.s.l. near Kaczyc e caused the Olza stages when flow was reduced. Thin litho fa cie s SGp were River fan be ing a com plex form, which was split into two proba bly as so ci ated with second- rank chan nels with flows parts in its dis tal zone. of lower energy. The se ries was depos ited un der very cold cli matic con - diti ons. It is evidence d by the pres ence of ice-wedges indi - METH OD OL OGY cat ing oc cur rence of per ma frost.

The study is based on litho fa cie s analy sis. A three-fold (2) Com plex of gla cio genic de pos its divi sion of de posi ti onal units is used, with a dis tincti on of In the NE part of the expo sure the lower gravels are li tho fa cies, fa cies as so cia tions and se ries. Li tho fa cies as so - covered with the SFh, FSh, SFr asso cia tion of sandy and cia tions dis tinguishe d in the se ries are denoted by code sym - sandy-sil ty sedi ments (Fig. 2). The asso cia tion’s thickness bols of the most fre quent beds. These sym bols are explai ned increa ses to the north from about 1.5 m to about 3.5 m over in Ta ble 1. The code is based on modifie d Mi all’s (1978) a dis tance of 100 m. The lower part of the asso cia tion con- code. sists of fine-grai ned sands and silty sands with horizon tal lamina ti on (Sh, SFh), and ripple cross-lam ination (SFr). They are overlai n by litho fa cie s of silty sands and sandy LO CATION OF THE SITE silts with hori zon tal lami na tion (SFh, FSh). Li tho fa cies of massive diam icton Dm, up to 0.5 m thick, is found local ly in The study site is situated in a gravel- pit at Koñc zyce, at the upper part of the asso cia tion (Fig. 2). The upper erosio- the right side of the small Pio trówka River val ley. The lat ter nal surface of the asso cia tion is topped with a layer of gravel is one of many erosiona l dissec tions cut ting the highplai n pave ment con tain ing Scandi na vian ma te rial (Fig. 3E). surface . The study site is locat ed about 3 km to the east of The sedi ments are char acter ized by oc cur rence of dif - the Olza River val ley, and about 10 km to the north of the fer ent scale de for ma tions. The small de for ma tion struc tures Car pa thian Foot hills (Fig 1). are usuall y drag folds with ver gence to the south. They are 42 T. SALAMON & A. WÓJCIK e t i s

e c y z c ñ o K

e h t

m o r f

s g o l

y r a t n e m i d e S

. 2

. g i F DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 43

Fig. 3 The Koñczyce site. A – sed i ments of the SE part of the site: 1 – lower se ries of gravel (se ries 1), 2 – till (se ries 2), 3 – se ries of flu vial sand (se ries 3), 4 – up per se ries of gravel (se ries 5); B–D – de posits of the lower se ries of gravel: B – lithofacies of massive gravel and sandy gravel dom i nated in the se ries (scale is 50 cm); C – medium-scale grav elly sand with lo cally high fre quency, usu ally oc cur as single beds or rare in small cosets, alter nately with thin beds of mas sive gravel (scale is 50 cm); D – ice-wedge struc tures de vel oped in two ho ri zons, filled with massive sand grav elly de posits; E–G – de posits of the glaciogenic complex: E – glaciolacustrine se ries built up of silts and sands. Me dium-scale re cumbent fold is vis i ble in the upper part of the se ries. Fold is ori ented to the south. Gravel pave ment with Scandi na vian mate rial occurred above the erosive surfaces of the series (marked by arrows ); F – close-up view of the glaciolacustrine de - posits. Silty sands or sandy silts with hor i zon tal lami na tion or rip ple-cross lam i na tion (in the lower part of the photo) are vis i ble. Ripplemarks migrated to the south. Small-scale drag folds are also visi ble; these are ori ented to the south as well; G – thin bed of basal till (arrowed) 44 T. SALAMON & A. WÓJCIK DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 45

found at several levels , and form disti nct hori zons with the (3) Serie s of sands thickness of 5–15 cm (Fig. 3F). Much greater ones oc cur in The erosiona l pave ment topping the gla ciogenic com - the upper part of the asso cia tion. Most fre quent are recum - plex is covered with a discon ti nuous com plex of sandy and bent folds about 2–2.5 m high and with vergence also to the sandy-gravel depos it s (Figs 2, 3A). Its thickness varies from south (Fig. 3E). 0.5 to 3 m. The serie s is mostly com posed of sands (more In the southern part of the expo sure, the lower gravel rarely grav elly sands and grav els) with large- scale pla nar serie s is overlai n by a thin (up to 1.5 m) cover of glacio flu - cross-stra tification Sp, (SGp) (Fig. 4A). They are usuall y vial sand and till (Figs 2, 3A). The till is silty- sandy dia mic- ac com pa nied by me dium- or small- scale li tho fa cies of ton, which forms a conti nuous, ca. 0.5–0.7 m thick layer sandy gravels or gravell y sands with horizon tal strati fica - (Fig. 3G). The diam icton has massive struc ture and many tion SGh or massive struc ture SGm. In the lower part of this sandy in ter lay ers and lenses. Fab ric meas ure ments in di cate se ries, silty clasts were ob served (Fig. 4B). The azi muths of a strongly preferred orien ta ti on of gravel clasts. The diam ic- cross- stratification dip in di cate that pa laeo cur rents flowed ton is covered with erosiona l pave ment, i.e. over ten cen ti- towards the N/NE (Fig. 2). metre s thick layer of gravels and sands with a consid er able The sedim ents were de posit ed in the envi ron m ent of a con tent of Scan di na vian ma te rial. The same pave ment over - sand-bed braided river, what is evi denced by high fre- lies the silty-sandy asso cia tion in the NE part of the expo - quency of Sp and SGp litho fa cie s. These litho fa cie s repre - sure (Fig. 2). sent mid-chann el trans verse bars ac creting down stream Sandy-sil ty asso cia tion SFh, FSh, SFr was depos it ed in (McDonald & Baner jee, 1971; Smith, 1972; Cant, 1978; a small, shal low gla cio mar gi nal lake. The li tho fa cies Sh, Cant & Walker, 1978). The li thofa cie s SGh and SGm were SFh, SFr, occur ring in the lower part of the asso cia tion, depos it ed from super cri ti cal flows as the sheets in the shal- were de rived from a shallow near-shore zone of the lake, in low zones of channels . In com pari son with serie s (1), this which the mate rial de liv ered by riv ers was spread over the se ries was as so ciated with a river sys tem of con sid era bly lake bottom by weak current s. The li thofa cie s SFh, FSh, oc- lower com petenc e. However, it was also de posit ed under curring in the upper part of the sec tion, was formed in a cold cli mate condi ti ons. It is confirm ed by num erous soft- somewhat deeper lake char acter ized by lower en ergy. In sediment clasts, espe cially sandy ones, which were trans - that lake, the sedi ments were de posit ed not only by peri odic ported as frozen elem ents (Fig. 4B). current s but also settl ed from suspen sion in alm ost stagnant wa ter. The direc tions of pa laeo flows in di cate that the lake (4) Lower se ries of silts was fed from two di recti ons, both from the north and south. The se ries of much finer-grai ned sedim ents is found in An ice-shee t was the southern source of supply . It was also the southern part of the expo sure, close to the axis of the the main cause of the lake origin. The lake was formed be- Pio trówka River val ley. The sediments fill a shal low (up to cause the channels of the northwardl y flowing Olza River 5 m) and wide (at least 70 m) trough (Figs 2, 4C). These are were dammed by ice masses. sands, silty sands, sandy silts, and silts char acter ized by al - Dia mic tic li tho fa cies, oc cur ring within the gla cio la cus - ter nate oc cur rence of lami nae of dif fer ent thick nesses and trine depos it s, are flow tills re depos it ed into the pond from grain sizes (Fig. 4D). In other places their structure is mas- the ice sheet sur face. De for ma tion struc tures, es pe cially the sive. The top of these sedim ents is erosiona l. The upper part ho ri zons of small folds, are as so ci ated with these tills. of the suc ces sion con sists of or ganic clayey silts reach ing Larger struc tures of overturne d folds were formed probably the thickness of 1–1.3 m in the axis of the trough and thin - by the ice sheet ad vanc ing over gla cio la cus trine de pos its. ning out towards its margins (Fig. 4C). These silts contai n The conti nuous layer of dia micton in the SW part of the nu mer ous plant mac ro rem nants and pol lens. Pa laeo bo tani- expo sure is a ba sal till depos it ed by the advanc ing ice sheet. cal analysis pre sented by Wójcik et al. (2004) shows domi- Its sub gla cial ori gin is evi denced by a flat ba sal sur face, and nati on of decidu ous forest s at that time. espe cia lly by strongly pre ferred orien ta ti on of gravel clasts. The deposi ti on of the serie s was precede d by erosion, The pave ment over ly ing till and gla cio la cus trine de pos its, which caused the form ati on of a wide trough. Fine-grai ned which prim aril y also had to be covered by till, indi cat es that char ac ter of the in fill ing sedi ments in di cates that they were glacia l depos it s are strongly re duced by erosion. asso ci ate d with very low-energy flows and peri ods of water

Fig. 4. The Koñczyce site. A, B – se ries of flu vial sands: A – sands with planar-cros s strati fi ca tion (scale is 50 cm); B – sandy clast in the bed of fine-grained gravel trans ported as frozen el e ment (scale is 10 cm); C, D – series of lower silts: C – over all view on the frag ment of the se ries. Bot tom ero sive sur faces are visi ble. Lower part of suc ces sion is built up of al ter nately lami nated poorly sorted sands, sandy silts and silts. Up per part of suc ces sion is built up of silts; in their up per part or ganic silts oc cur (ar rowed); D – close-up view of the mar- ginal part of lower se ries of silts. Bot tom ero sive sur faces are emphasised by gravel pave ment (ar rowed); above lami nated sandy and silty sed i ments are vis i ble; E–I – upper se ries of gravel: E, F – over all and close-up view of the se ries in the south ern part of site; G – distinct ero sive sur faces sep a rated two gravel units. The lower unit is strongly de formed with the sands of the un der ly ing se ries and cut by the up - per one; H – well rounded silty clasts in the bot tom part of the gravel se ries; I – strongly scored lens of silts (marked by ar rows). Above, ir - regu lar silty clasts (marked by dot ted lines) are also visi ble 46 T. SALAMON & A. WÓJCIK

Fig. 5. Up per se ries of silts. A – poorly sorted massive sands, alter nately with thin laminae of silts, occur locally in the lower part of the series (scale is 50 cm); B – slightly de formed sandy and silty lithofacies with dis tinct vergence of de for mation struc tures to the north; C – massive sandy silts with dis persed gravel clasts; D – silts of the up per part of the se ries. Or ganic ho ri zons are ar rowed

stag na tion. The al ter nate oc cur rence of sedi ments of dif fer - from 1 to more than 20 cm, their shape is irregu lar and ent grain sizes and their poor sorting, espe cia lly in the rounded (Fig. 4H). Concen tra tion of the clasts is the largest trough marginal parts, indi cat e the high content of slope de- in the 1-m -thi ck band extend ing over erosive surface s of the posit s washed into the erosiona l dissec tion. Organic silts series . How ever, irregu lar silty fragm ents were also ob- were ac cu mu lated when flow com pletely ceased. Litho logi - served in other parts of the serie s (Fig. 4I). Sandy litho fa cie s cal charac ter of sedi ments and high content of organic mate - were also noted in the se ries, but their frequency is much rial suggest that the serie s was depos it ed under warm cli - lower than the gravel ones. These are thin, elongate d lenses mate con di tions. Wójcik et al. (2004) inter preted the pollen of massive sands Sm (Fig. 4E, F). Rare ele ments of the se - suc ces sion as an in ter gla cial one (Cro merian I). ries are len ticu lar beds of planar cross- stratified sand Sp with very low lat eral ex tent (1–2 m) and massive silts Fm (5) Upper se ries of grav els (Fig. 4F, I). Erosiona l surface s have been local ly noted The serie s of gravels reaches the thickness of 5–6 m. It within gravel packages (Fig. 4G). In places the gravels are is com posed of litho fa cie s asso cia tion Gm (Sm, Gl). The se - deform ed with the sands of under ly ing se ries (Fig. 4G). ries covers an erosiona l surface , local ly in the form of shal - The beds of se ries (5) are incli ned to the north at a low troughs (Fig. 3A). The asso cia tion consis ts mostly of slightly greater angle than the units of under ly ing se ries. In gravel li thofa cie s of massive struc ture Gm, usuall y of me- the NE part of the expo sure the gravels occur di rectly over dium or large scale. The li tho fa cies thick ness is from a the pavem ent topping glacio genic sedi ments. The serie s of dozen or so to over 50 centi metre s (Fig. 4E, F). These are flu vial sands is alm ost completely reduced in these places. mostly matrix-supporte d gravels . The mean gravel size is The dominance of litho fa cies Gm indi cates a con nec - 2–6 cm. Lo cally, in the lower part of the se ries, large- scale tion of the sedi ments with the envi ron m ent of gravel-bed gravel or sandy gravel with planar, usuall y low-angle braided river (Wil liams & Rust, 1969; Smith, 1970; Rust, cross-stra tification Gl are observe d. The gravels usuall y 1972; Miall , 1977). They were mostly depos it ed as longi tu - built infil lings of trough struc tures. In the basal part of se- dinal bars and gravel sheets under condi ti ons of upper flow ries, the grav els con tain abun dant silty clasts. Their size is re gime. The thick est li tho fa cies Gm are iden tified with the DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 47

longi tu di nal bars. Lack of litho fa cie s which could be relat ed Load cast struc tures occur at the con tact of loess with the to lower flow regim e suggest s that all channels of the fluvial un der ly ing de pos its. sys tem were shallow. Poor sorting and massive struc ture of In Jersak’s (1983), opinion the menti oned sedim ents to- grav els in di cate rapid de po si tional pro cesses. Sud den re- gether with under ly ing silts of se ries (6) rep re sent one stra - ducti on of flow com petenc e in the fi nal phase of flood en- tigraphic hori zon of the last glacia tion. Wójcik et al. (2004) abled deposi ti on of sands. They usuall y formed thin sheets and Drewnik et al. (2004) dis cern frag men tar ily pre served in the secon dary channels . ini tial pa laeo sols in the loess se ries, which point, in their Cross- stratified grav els in fill ing scours in the lower part opinion, to differ ent ages of sedim ents. of the series were derived from deeper chan nel zones, which functi oned during river surges onto the previ ously inac ti ve plain. The chan nel flows were char acter ized by high ero sive DE VEL OP MENT po ten tial. In ten sive ero sion dur ing that ini tial pe riod of se- OF THE OLZA RIVER FAN ries devel op m ent can be inferred also from a large number of sedi ment clasts in the bot tom part of the serie s. Sedimentological model The pres ence of channel- like ero sional sur faces and abundant frequency of massive silts within the channels in- The predomi nance of flysch mate rial in di cates that the fills suggest frequent episodes of avulsion in the fluvial sys - ex am ined grav els (series 1, 5) were transported from the tem. These types of sedi ments were ac cu mu lated proba bly Car pa thian Mts. by the Olza River. The occur rence of grav - quite com monly in the system , but usuall y were eroded dur- els at a dis tance of sev eral kilo metres from the pres ent val - ing later flood flow events. It is confirm ed by the pres ence ley of the Olza River shows that the river freely migr ated, of num erous clasts and irregu lar fragm ents of silts in the where it left the Car pa thian Foothills. The wide lat eral gravel li tho fa cies in dif fer ent part of the se ries. Avul sion spread of grav els ap pears to in di cate that they were de pos - caused that some channels under went sudden abandon m ent ited as a fan (Fig. 6A). This sedim entar y envi ron m ent is also and other ones were trenched in the same time. in ferred from rela tively small thick nesses of suc ces sive se - ries. For ex am ple, the up per se ries of gravel, cor re lated with (6) Up per se ries of silts one gla cial period, is only 5–6 m thick. In com pari son, the Gravel series (5) is overlai n by fine-grai ned depos it s, thickness of allu via building the terrace s in the mountai n 1.2 to 3.5 m thick (Fig. 2). The lower part of the serie s is and foot hill val leys reaches often more than a dozen or so char ac ter ised by a high lat eral vari abil ity. Dia mic tic mas - metre s (Starkel, 1977). Small thickness of the studied serie s sive sandy silts with scattered gravel clasts dominate lo cally can be explai ned by inten sive lat eral migra ti on of the river (Fig. 5C). In other places small- or medium-sca le beds of channels on a broad fan surface . Frequent avulsion is inter - poorly sorted massive sands have been noted. The sands preted from num erous marks of fragm entar ily pre served contai n rare granules and the silt laminae of various thick- sedi ments depos it ed in abandoned channels . It is also con- nesses (Fig. 5A). The frequency of silt inter cala ti ons in- firmed by ice- wedge struc tures devel oped at dif fer ent lev - creases to wards the top of the se ries. Sandy- silty sedim ents els. These indi cat e peri ods of vari ous fluvial acti vit y in indi - are often de formed (Fig. 5B). The se ries repre sent s a fining- vidual parts of fan surface s, what is typi cal for al luvial fans. upward suc ces sion. The upper part of the serie s is predom i- Li tho fa cies char ac ter of the se ries in di cates that the fan nated by massive silt. Few thin hori zons of brown organic was mostly aggraded in cold pe riods when the river system silts oc cur there (Fig. 5D). Rich as semblag es of flo ris tic acted as a braided pat tern. Great supply of depos it s to river rem nants and pollen of ther mophi lous plants have been channels in the mountai n sec tion of the valley , asso ci ate d found in this part of sedim entar y secti on (Wójcik et al., with disap pear ance of a forest cover, result ed in river over- 2004). load ing and in ten sive depo si tion. The ba sal part of the serie s is com posed of fluvial sedi - The form ati on of fans by rivers leaving mountai n areas ments depos it ed most proba bly in an overbank zone. Sand was very com mon phenom enon in cold peri ods (Ksi¹¿kie- beds de rived from short-li ved flows and all fine-grai ned li - wicz, 1935; Stupnicka, 1963; Starkel, 1967; Gi lot et al., thofa cie s were mostly settl ed from suspen sion. Frequency 1982; Niedzia³kowska et al., 1985; Krzysz kowski, 1993; and in ten sity of cur rents de creased pro gres sively dur ing Mastal erz & Wo jewoda, 1993; Badura et al., 2005). Narrow sedi menta ti on of this serie s. The upper part of the serie s was mountai n valley s were predis posed to fast aggra da ti on of al - formed in stagnant water s. Re sults of pollen analy sis reveal lu via. This re sulted in a con sid er able in crease in in cli na tion the high vari abil ity of flora. The pollen spectra point to two of deposi ti on surface at the val ley outlet to the foreland, warm peri ods, which made Wójcik et al. (2004) to be lieve which is typi cal for fan envi ron m ent. Loca ti on of the site in- that the studied serie s might corre spond even with two in - dicat es that the studied sedim ents were de posit ed in the tergla cia l stages (Cro merian II–III). Accord ing to Jersak middle or even more distal part of the fan. (1983), organic depos it s were formed in tundra condi ti on Flu vial ac tiv ity of the fan ceased when river started to during the Vistul ian. cut into its surface . In opinion of many resea rchers (Rose, 1995; Kasse et al., 1995; Mol, 1997; Huisink, 1997, 2000; (7) Serie s of loess-li ke depos it s Mol et al., 2000; Vanden berghe, 2002; Kasse et al., 2003), The silt se ries is cov ered with loess de pos its. Their this proces s occurred in European river system s in the fi nal thick ness reaches a dozen or so metres. The loess is usu ally stages of glacia tions and re sulted in de crease of de posit sup- laminate d in the lower part and massive in the upper one. ply to river channels , and led to erosion. The disap pear ance 48 T. SALAMON & A. WÓJCIK

Fig. 6. Model of the Olza River fan’s de vel opment. A – fan de vel op ment under cold cli mate con di tion dur ing gla cial stages. The entire fan sur face was aggraded by grav els and sands in a braided river system; B – fan de vel op ment in fi nal phases of glaciations and dur ing interglacials under warm climate con ditions . Main river activ ity was restricted to a narrow valley, which deeply dissected the fan surface. Out side part of the fan, slightly dissected by sec ondary val leys, was colo nised by for est. These val leys were filled with fine-grained sed i - ments; C – fan de vel opment under cold cli mate con di tion af ter tec tonic up lift and/or dur ing lower in ten sity of de posi tion. Flu vial processes re stricted to smaller fan in serted in the older, dis sected form. In ten sive ae olian loess depo sition on higher sur faces of the in ac - tive part of the fan of perm afrost played also a consid er able role (cf. Huisink, form of a braided pat tern again. Gradual disap pear ance of 2000; Mol et al., 2000; Vanden berghe, 2001, 2002). At that forest s precede d the aggra da ti on of the fan surface with the time, the Olza River probably changed its pat tern into one- suc ces sive se ries of gravel al lu via. Grav els were de pos ited channel system . Such pro cess was re corded in many valleys on the fan sur face af ter filling the Olza River in ci sion. In during the end of the last glacia tion (Starkel, 1977; Szu - this way, the avulsion of channels and their uncon fine d mi- mañski, 1986; Kozar ski, 1983; Kasse et al., 1995; Mol et grati on on the fan surface were pos sible. al., 2000). In this way the river reduced its acti vit y to a nar- There were proba bly sev eral such accumulational- row dissec tion of the fan. This zone evolved with time into a erosional cycle s during the devel op m ent of the Olza River flat- bottom river val ley, like the pres ent Olza River val ley. fan. However, precis e deter mina ti on of their number is im - From the time when the river system had changed and possi ble. Espe cia lly, the lower se ries of gravels is poorly the Olza River started downcut ti ng, the fan was not ag- ex am ined be cause of their frag men tary ex po si tion. This graded with al luvia but fluvial proces ses on its surface were thick se ries can be multi par tite. Wójcik et al. (2004) as- not com pletely stopped. Those parts of the fan, which were sumed that it can rep re sent even tri par tite di vi sion. out side the Olza River tract, be came the places of activ ity of Presum ably , the fan evolu ti on was much more com pli - sec on dary streams – the tribu tar ies of the Olza River (Fig. cated than the present ed model. It is very probable , for ex- 6B). These small streams also cut the fan sur face. How ever, am ple, that the apex of the fan was shifted to the north dur- that pro cess oc curred much slower and on a smaller scale, ing the suc ces sive cold pe riods, due to differ ent levels of ag- be cause the en ergy of small streams was low. Their ac tiv ity grada ti on of the Olza River val ley. This phenom enon oc- result ed in form ati on of the sys tem of narrow and shallow, curred when aggra da ti on of al luvia in the valley reached a small val leys, which dissected the fan sur face. One of such lower level than in the former peri ods (cf. White et al., erosiona l dissec tions is recorded in the studied site as a 1996). Unfor tu nate ly, no geom orphic tool can be used in channel struc ture filled with fine-grai ned sands and silts (se- this study, be cause the fan is covered by thick loess-li ke de- ries 4). pos its, and the primary flu vial re lief is bur ied. The val ley system , de scribed above, was being es tab - A quite dif fer ent fan de vel op ment oc curred dur ing the lished dur ing the in ter gla cial stages. The fan sur face was gla cial pe riod, when the ice sheet ad vanced on the ex am ined colonize d by plant com muni ti es. Low acti vit y of fluvial re gion. The ice sheet cov ered the whole area of the Ci eszyn pro cesses, limited to nar row, sec on dary val leys is reflected Foothil ls, and reached its maxim um extent a dozen or so in the suc ces sion of serie s (4). Fine-grai ned nature of the de- kilo metres to the south of the Koñczyce site (Ksi¹¿kiewicz, posit s indi cat es their connec ti on with low-energy flows, and 1935; Klim aszewski, 1952). The fan surface was built up by peri odi cal ly even with the deposi ti on in com pletely stagnant till and gla cio flu vial de pos its. Lo cally, small, dammed lakes wa ter. It was probably as so ciated with the occur rence of lo - exist ed in the fan zone in the front of advanc ing ice-shee t. cal wa ter logged ar eas with stag nant wa ter in a small valley. Sandy and sand-sil ty depos it s ac cum ulat ed in these shal low The deposi ti on took place under warm cli mate condi ti ons as ponds. evidence d by the occur rence of organic silts with pol len and The se ries (3) occur ring di rectly over the gla ciogenic rem nants of ther mo phi lous plants, es pe cially de cidu ous depos it s differs from the other ones. It is com posed not of trees (Wójcik et al., 2004). gravels but mostly of sands. The NE direc ti on of palae o - En vi ron men tal con di tions of the fan proba bly changed flows in di cates con nec tion of the se ries with the Olza River, in consec uti ve cold peri ods. The Olza River system took the the same as the gravel units. Pre sumably, the source mate - DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 49

rial of these sands were mainly glacial de pos its re de pos ited analy sed organic silts and the com plex of glacio genic de- from the foothills sec tion of the Olza River val ley. Be cause posit s are stra tigraphic key lay ers in the de posit s under of indi vid ual charac ter of the serie s com pared to gravel allu - study. Accord ing to Jersak (1983), the organic depos it s vial units, deter mina ti on of the mom ent of its deposi ti on is overly ing the upper gravels are of Vistul ian age, pointing to very dif fi cult. It is pos si ble that this se ries was as so ci ated a long pe riod of fan acti vit y and indi cat ing that the Odranian with some cold period of lower rank, which occurred after (Saalian-1) Gla ciation might have been the last stage of al- the main phase of glacia tion, or even with the phase of ice- luvial fan building up. This hy pothesis is well explai ned by sheet re treat. the fact that the end of fan’s flu vial ac tiv ity fol lowed the ac - The upper m ost serie s of gravels was asso ci ate d with the cu mu la tion of up per gravel (se ries 5). In this way, the ces sa - succes sive stage of fan building up during the next glacia - tion of fluvial aggra da ti on can be inter preted as: re acti on to tion. Sands and silts occur ring in its top part repre sent the iso static move ments that oc curred af ter the Odra nian Gla - last epi sode of fluvial deposi ti on on the fan, mostly from ciation, when the ice sheet ad vanced as far as the north ern sus pen sion. They were proba bly de pos ited in sec on dary boundary of the Moravi an Gate (Le wandowski, 1988), channels of streams flowing on the fan surface during and/or lower inten sit y of deposi ti on in the Olza River valley greater floods, when the Olza River started to dis sect its dur ing suc ces sive gla cia tions (War ta nian, Vis tulian). How- own al luvia. Flow routes started to concen tra te in the main ever, the result s of other studies (Wójcik et al., 2004) sug- val ley, which deep ened at that time. How ever, ero sion was gest that the acti vit y of fluvial proces ses finishe d much ear- so slow that, for some time, the river could have overflowe d lier, i.e. be fore the Sanian Glacia tion (Elsterian-2). This as - the surface of the dissec ted fan during floods. Fine grain sumpti on seems to be surpris ing in the context of subse - size of depos it s indi cat es that energy of flow was rather low, quent glacia tions (Sanian and Odra nian), during which the and transport oc curred mostly in suspen sion. The tem porary ice sheet advance d far to the south (Le wandowski, 1988; overbank flows, probably asso ci ate d with great floods, rap- Macoun & Králik, 1995; Marks, 2005; Mojski, 2005). The idly turned into the phases of stagnant water . In later peri - questi on has to be asked: why the Olza fan did not undergo ods, these pe ri odi cally active parts of the fan be came the al lu vial ag gra da tion in con di tions of peri gla cial cli mate and places where silts and or ganic de pos its accu mu lated. They prox im ity of ice sheet fa vour ing in ten sive ac cu mu la tion are very well preserve d, mostly owing to the fact that during during the menti oned gla cia tions, es pecia lly that the val leys the succes sive cold stage the fan’s building up with al luvia, of Carpa thi an rivers aggraded then very inten sive ly (Kli - usuall y pre ceded by erosion, did not occur. maszewski, 1948; Starkel, 1972). Wójcik et al.‘s (2004) Loess-li ke sedim ents were de posit ed by wind under the stra tigraphic in ter pre ta tion raises also an other ques tion: peri gla cial cli mate con di tions. Dur ing their ac cu mu la tion why two se ries of in ter gla cial age (se ries 6) are not sepa - the fan was not cov ered with suc ces sive se ries of grav els. rated by a hori zon of peri glacia l structure s or any evident Most probably , fluvial acti vit y on the fan had to be confine d erosiona l surface s, in a such dy namic zone like the fore- to a narrow zone (Fig. 6C). Aggra da ti on in the Olza River mountain area? valley was too small for river overflow ing the fan surface . All these ques tions and doubts order to keep great cau- This can suggest the lower inten sit y of deposi ti on. On the tion for strati graphic inter preta ti on of the fan depos it s. If we other hand, the same effect could have been brought by the as sume the uni ver sally ac cepted opin ion about gla cia tion of upli ft of substra tum caus ing rise of the fan surface and the the Carpa thi an foreland dur ing the Sanian (Elsterian-2) Gla - change of its hy dro logi cal con di tion. Neo tec tonic ac tiv ity of cia tion (Kli maszewski, 1952; Lindner, 1992; Mojski, 1993, the area during the fan for mati on is suggest ed by the discor - 2005; Macoun & Králik, 1995; Marks, 2005), it can be con- dant oc cur rence of suc ces sive se ries. The series of up per cluded from the succes sion of the se ries, that the upper se - gravels is incli ned to the north at a slightly greater angle ries of gravels should have been depos it ed during the Odra- than the older ones. Verti cal movem ents could have been nian (Saalian-1) Gla cia tion. The un der ly ing and over ly ing as so ci ated with iso static re laxa tion of the sub stra tum due to serie s in this concept would be, respec tively, older and the re treat of the Scan di na vian ice sheet. Such phe nomena younger. This suppo si ti on is still in contra dicti on to the re- are com monly docum ented from the Sudetes foreland (Dy- sults of paly no logi cal and pa laeo mag netic analy ses (Wójcik jor, 1983; Krzysz kowski & Stachura, 1998) and from the et al., 2004), which are diffi cult to challenge . Finall y, it can South-Poli sh Uplands (Liszkowski, 1993). The arrange - be con cluded that in such mor pho logi cally di ver si fied re- ment of layers in di cates that the ampli tude of up lift in - gion any analyses can not be uncri ti cally used for stra - creased to the north. After deposi ti on of the upper gravel se - tigraphic in ter pre ta tion with out con sid er ing all po ten tial ries the area was again slightly upli fted. This is proved by data. In the light of contem porary studies the age of the Olza the ge ology of the pres ent valley bottom s of the Olza River fan is still far from unam bigu ous infer ence and can be and its tribu tar ies. These riv ers are in cised sev eral metres younger than Wójcik et al. (2004) have suggest ed. deep into the Mio cene clays (Wójcik et al., 2004).

FI NAL RE MARKS Strati graphic con straints A funda m ental questi on in the Olza River fan’s devel - Sedi ments in the Koñc zyce site were de pos ited mainly op ment is stra tigraphic cor re la tion of suc ces sive units. The by the Olza River in the zone of a fore-m ountain fan, at the con se quences of their in ter pre ta tion have widesprea d in flu - val ley outlet from the Car pa thian foot hills. The fan was ence on the palaeogeog ra phy of the region. Paly nologi cally formed in many stages. Lithologi cal differ en ti ati on of the 50 T. SALAMON & A. WÓJCIK

Ta ble 2 Com par i son of con sec u tive phases of fan de vel op ment

Series of deposits Climate conditions Environment of sedimentation Phase of fan development Aeolian deposition of fine-grained Aggradation of loess on the higher (7) Series of loess Cold climate conditions (glaciation) deposits part of fan surfaces The lower part of series connected with overbank deposition of fluvial Low-energy deposition in the Transition from cold to warm, finally (6) Upper series of silts system. Silts of the upper part of abandon channel system on the fan warm climate conditions succession deposited in stagnant surface water condition Fluvial aggradation of alluvia on the (5) Upper series of gravels Cold climate conditions (glaciation) Shallow gravel-bed braided river fan surface Low-energy small fluvial system In the first phase transition from cold Dissection of the fan surface and (tributary of the main river), (4) Lower series of silts to warm, later warm climate low-energy deposition in the occasionally deposition in stagnant conditions secondary palaeovalleys water condition Cold climate conditions (glacial Fluvial aggradation of alluvia on the (3) Series of fluvial sands Sand-bed braided river stadial?) fan surface (2) Complex of glaciogenic Glaciomarginal and subglacial Glaciogenic aggradation on the fan Cold climate conditions (glaciation) sediments deposition surface Fluvial aggradation of alluvia on the (1) Lower series of gravels Shallow gravel-bed braided river fan surface stud ied sedi ments re flects great vari abil ity of de po si tional fault zones: an ex ample of al lu vial fan cor re la tion from the condi ti ons (Ta ble 2). The fan evolu ti on was mainly con - up per Qua ter nary of the south ern Po Ba sin, It aly. Sed i men - trolled by Pleis to cene cli matic changes. tary Ge ol ogy, 102: 275–295. Un der cold cli mate con di tions dur ing gla cia tions, the Badura, J., Kowalska, A., Przybylski, B. & Dobosz, T., 2005. fan surface was built up mainly of the se ries of gravels de- Osady sto¿ka nap³ywowego Bobru: przyk³ad akumulacji rzecznej w warunkach strefy peryglacjalnej. (In Polish). In: posit ed by a shallow braided river. Gravels were de posit ed Terenowe Warsztaty Sedymentologiczne SUDETY 2005. Spe- mostly as longi tu di nal bars and sheets. The channels were cyfika plejstoceñskiej sedymentacji gór i wy¿yn, Sudety, 5-9 charac ter ized by fre quent avulsion. In the final phases of wrzeœnia 2005. Instytut Nauk Geologicznych Uniwersytetu cold pe riods the fan was dissec ted, and the acti vit y of the Wroc³awskiego, Pañstwowy Instytut Geologiczny, Komisja Olza River be came re stricted to a nar row val ley. Besides the Litologii i Genezy Osadów Czwartorzêdowych Komitetu main river the fan was dis sected also by secon dary streams, Badañ Czwartorzêdu PAN, Wroc³aw: 47–61. the tribu tar ies of the Olza River. Dur ing in ter gla cials the fan Beaty, C. B., 1963. Or i gin of Al lu vial fans, White Moun tain, Cal i - was only slightly transform ed. Geody nam ic proces ses acted for nia and Ne vada. An nals of the As so ci a tion of Amer i can only in the ax ial nar row, small val leys. The fan sur face was Ge og ra phers, 53: 516–535. colonize d by forest s. Blair, T. C., 1999. Cause of domi nance by sheetflood vs. de - A specia l period of the fan de velop m ent oc curred dur- bris-flow pro cesses on two ad join ing al lu vial fans, Death Val - leys, Cal i for nia. Sedimentology, 46: 1015–1028. ing the gla cia tion when the ice sheet advance d on the Carpa - Blair, T. C. & McPherson, J. G., 1994. Al lu vial fans and their nat - thian fore land. The fan becam e then a place of gla cio genic u ral dis tinc tion from rivers based on mor phol ogy, hy drau lic depo si tion. Neo tec tonic move ments were proba bly an im - pro cesses, sed i men tary pro cesses, and fa cies as sem blages. portant factor in fan’s de velop m ent. These small-am plitude Jour nal of Sed i men tary Re search, 64: 450–489. move ments could have pre suma bly been as so ci ated with Boothroyd, J. C. & Nummedal, D., 1978. Proglacial braided iso static re laxa tion of the sub stra tum af ter the re treat of the outwash: a model for hu mid al lu vial-fan de posits. In: Miall, Scan dina vian ice sheet. Aggra da ti on of the fan was ter mi- A. D. (ed.), Flu vial Sedimentology. Ca na dian So ci ety of Pe - nated most proba bly due to upli ft of the area. A consid er - tro leum Ge ol o gists, Mem oir, 5: 641–668. able part of the fan be came the place of aeo lian ac cu mu la- Budek, A., Drewnik, M. & Kacprzak A., 2004. Micromorphology tion of loess at that time. of the silt sedi ments at the Koñczyce profile (Kotlina Oœwiê- cimska). (In Pol ish, Eng lish summary ). Biuletyn Pañstwo- wego Instytutu Geologicznego, 409: 63–74. Ac knowl edge ments Cant, D. J., 1978. De vel opment of a fa cies model for sandy braided river sed i men ta tion: com par i son of the South Sas- We thank T. Zieliñski for criti cal re view of the manuscript katch e wan River and the Bat tery Point Forma tion. In: Miall, and T. Mrozek for lin guistic cor rec tion of the text. A. D. (ed.), Flu vial Sedimentology. Ca na dian So ci ety of Pe - tro leum Ge ol o gists, Mem oir, 5: 627–639. REF ER ENCES Cant, D. J. & Walker, R.G., 1978. Flu vial pro cesses and fa cies se - quences in the sandy braided South Saskatchewen River, Amorosi, A., Farina M., Severi, P., Preti, D., Caporale, G. & Dio, Can ada. Sedimentology, 25: 625–639. D., 1996. Ge net i cally re lated al lu vial de pos its across ac tive DeCelles, P.G., Gray, M. B., Ridgway, K. D., Cole R. B., Pivnik, DE VEL OP MENT OF A FORE-MOUN TAIN AL LU VIAL FAN 51

D. A., Pequera N. & Srivastava, P., 1991. Con trols of synoro- cenie, okolicy Œwidnicy, Przedgórze Sudeckie. (In Polish). genic ar chi tec ture of Beartooth Con glom er ate (Paleocene), In: Baseny sedymentacyjne – procesy, osady architektura. Wy o ming and Montana. Sedimentology, 38: 567–590. Przewodnik 2 Krajowego Spotkania Sedymentologów, Drewnik, M., Kacprzak, A., Wójcik, A., ¯y³a, M. & Szeliga, W., Wroc³aw - Sudety, 4-7 wrzeœnia 1993. Wroc³aw: 47–64. 2004. Charakterystyka utworów py³owych w profilu Koñ- Krzyszkowski, D. & Stachura, R., 1998. Neotectonically con - czyce (Kotlina Oœwiêcimska). (In Polish, English summary). trolled fluvial fea tures, Wa³brzych Up land, Mid dle Sudeten Biuletyn Pañstwowego Instytutu Geologicznego 409: 51–62. Mts, south west ern Po land. Geo mor phol ogy, 22: 73–91. Dyjor, S., 1983. Evo lu tion of Ter tiary Grabens sit u ated be fore Ksi¹¿kiewicz, M., 1935. Über die Quartärbildungen im Teschener Cen tral and East ern Sudetes. (In Pol ish, Eng lish summary ). Hügellande. (In Polish, Ger man summary ). PAU Wydaw- In: Materia³y III Krajowego Sympozjum “Wspó³czesne i nictwa Œl¹skie - Prace Geologiczne, 2: 1–16. neotektoniczne ruchy skorupy ziemskiej w Polsce”, IV, Lewandowski, J., 1988. Middle Pleis to cene in the up stream Odra Ossolineum, Wroc³aw: 155–181. val ley re gion: – Racibórz Ba sin (syn thet i cal Gilot, E., Niedzia³kowska, E., Sobolewska, M. & Starkel, L., ap proach). (In Pol ish, Eng lish summary ). Przegl¹d Geolo- 1982. Pleniglacial allu vial fan of the Bia³a Stream at Kaniów giczny, 36: 465–474. near Czechowice (The Oœwiêcim Basin). Studia Geomor- Lindner, L. (ed.), 1992. Czwartorzêd, osady, metody badañ, stra- phologica Carpatho-Balcanica, 15: 115–124. tygrafia. (In Pol ish). Wydawnictwo Polskiej Agencji Ekolo- Guzzetti, F., Marchetti, M. & Reichenbach, P., 1997. Large allu - gicznej, Warszawa: 1–683. vial fans in the north-cen tral Po Plain (North ern It aly). Geo - Liszkowski, J., 1993. The effect of Pleisto cene ice-sheet load- mor phol ogy, 18: 119–136. ing-deloading cy cles on the bed rock struc ture of Po land. Harvey, A. M., 1996. The role of al lu vial fans in the mountain flu - Folia Quaternaria, 64: 7–23. vial sys tem of southeast Spain: impli ca tion of climate change. LÝnne, I. & Nemec, W., 2004. High-arc tic fan delta re cord ing Earth Surface Pro cesses and Landforms , 21: 543– 553. deglaciation and en vi ron ment dis equi lib rium. Sedimentology, Harvey, A. M., Silva, P. G., Mather, A. E., Goy, J. L., Stokes, M. 51: 553–589. & Zazo, C., 1999. The impact of Qua ter nary sea-level and cli - Macoun, J. & Králik, F., 1995. Gla cial history of the Czech Re - matic changes on coastal al lu vial fans in the Cabo de Gate pub lic. In: Ehlers, J., Kozarski S. & Gibbard, Ph. (eds), Gla - ranges, south east Spain. Geo mor phol ogy, 28: 1–22. cial de posits of North-East Eu rope. Balkema, Rot ter dam- Heward, A. P., 1978. Allu vial fan se quence and megasequence Brookfield: 389–405. models: with ex amples from Westphalian D – Stephanian B Macoun, J., Šibrava, V., Tyraèek, J. & Kneblova-Vodièková, V., coalfields, N Spain. In: Miall, A. D. (ed.), Flu vial Sedimento- 1965. Quartär im Gebiet von und in der Mährischen logy. Ca na dian So ci ety of Pe tro leum Ge ol o gists, Mem oir, 5: Pforte. (In Czech, Ger man summary ). Ústøedny Ústav Geolo- 669–702. gický, Praha, 419 pp. Huisink, M., 1997. Late-gla cial sedimentological and morpho log i - Marks, L., 2005. Pleisto cene glacial limits in the terri tory of Po- cal changes in a low land river in re sponse to cli matic change: land. Przegl¹d Geologiczny, 53: 988–993. the Maas, south ern Neth er lands. Jour nal of Qua ter nary Sci - Mastalerz, K. & Wojewoda, J., 1993. Al lu vial-fan sed i menta tion ence, 12: 209–223. along an active strike-slip fault: Plio-Pleisto cene Pre- Huisink, M., 2000. Chang ing river style in re sponse to Weichse- Fan, SW Poland. Al lu vial Sed i men ta tion. In ter na - lian climate changes in the Vecht valley, east ern Neth erlands. tional As so ci a tion of Sedimentologists, Spe cial Pub li ca tion, Sed i men tary Ge ol ogy, 133: 115–134. 17: 293–304. Jersak, J., 1983. Osady w Koñczycach Ma³ych – formacja glin Mc Donald, B. C. & Banerjee, I., 1971. Sed i ments and bed forms lessowych. (In Pol ish). In: Przewodnik konferencji: “PóŸno- on a braided outwash plains. Cana dian Jour nal of Earth Sci - vistuliañskie i holoceñskie zmiany œrodowiska geograficz- ences, 8: 1282–1301. nego na obszarach lessowych Wy¿yny Miechowskiej i Opa- Miall, A. D., 1977. A re view of the braided-river depositional en - towsko-Sandomierskiej”. Komitet Badañ Czwartorzêdu vi ron ment. Earth Science Reviews , 13: 1–62. PAN, UŒ, Katowice: 35–38. Miall, A. D., 1978. Lithofacies types and verti cal profile mod els in Kasse, C., Vandenberghe, J. & Bohncke, S., 1995. Cli matic braided rivers: A summary. In: Miall, A. D. (ed.), Flu vial change and fluvial dy namics of the Maas dur ing the late Sedimentology. Ca na dian So ci ety of Pe tro leum Ge ol o gists Weichselian and Early Ho locene. In: Frenzel, B. (ed.), Eu ro- Mem oir, 5: 597–604. pean River Ac tiv ity and Cli matic Change Dur ing the Lategla- Mojski, E., 1993. Europa w plejstocenie – ewolucja œrodowiska cial and Early Holo cene. ESF Pro ject “Eu ropean Paleocli- przyrodniczego. (In Pol ish). Wydawnictwo Polskiej Agencji mate and Man”, Spe cial Is sue 9. Paläoklimaforschung/ Ekologicznej, Warszawa: 1–311. Palaeoclimate Resear ch, 14: 123–150. Mojski, E., 2005. Ziemie polskie w czwartorzêdzie. Zarys morfo- Kasse, C., Vandenberghe, J., Van Huissteden, J., Bohncke, S. J. P. genezy. (In Pol ish). Pañstwowy Instytut Geologiczny, & Bos, J. A. A., 2003. Sensi tiv ity of Weichselian flu vial sys- Warszawa: 1–375. tems to climate change (Nochten mine, eastern Ger many). Mol, J., 1997. Flu vial re sponse to Weichselian cli mate changes in Qua ter nary Sci ence Re views, 22: 2141–2156. the Niederlausitz (Germany). Jour nal of Qua ter nary Sci ence, Klimaszewski, M., 1948. Polish West Carpathians in the Ice Age. 12: 43–60. (In Polish, Eng lish summary ). Acta Geographica Universi- Mol, J., Vandenberghe, J. & Kasse, C., 2000. River re sponse to tatis Wratislaviensis, Ser. B, 7: 1–236. varia tion of periglacial climate in mid-lati tude Europe. Geo - Klimaszewski, M., 1952. The prob lems of the Pleis to cene in mor phol ogy, 33: 131–148. Southern Po land. (In Pol ish, Eng lish summary ). Biuletyn Nemec, W. & Postma, G., 1993. Qua ter nary al lu vial fans in south - Pañstwowego Instytutu Geologicznego, 65: 137–213. west ern Crete: sed i men ta tion pro cesses and geomorphic evo - Kozarski, S., 1983. River chan nel changes in the mid dle reach of lu tion. In: Marzo, M. & Puigdefabregas, C. (eds), Al lu vial the Warta River, Great Po land Low land. Qua ter nary Stud ies sed i men ta tion. In ter na tional As so ci a tion of Sedimentologists, in Po land, 4: 154–169. Spe cial Pub li ca tion, 17: 235–276. Krzyszkowski, D., 1993. Rozwój sto¿ków Bystrzycy w plejsto- Niedzia³kowska, E., Gilot, E., Pazdur, M. & Szczepanek, K., 52 T. SALAMON & A. WÓJCIK

1985. The up per val ley near Drogomyœl in the late Starkel, L., 1972. Karpaty Zewnêtrzne. (In Pol ish). In: Klima- Vistulian and Holocen. Folia Quaternaria, 56: 101–132. szewski, M. (ed.), Geomorfologia Polski, T.1. PWN, Niedzia³kowska, E. & Szczepanek, K., 1993–1994. Vistulian silty Warszawa: 52–115. sedi ments of the Vistula river fan in the Oœwiêcim Basin. (In Starkel, L., 1977. Last Gla cial and Holo cene flu vial chro nol ogy in Pol ish, Eng lish sum mary). Studia Geomorphologica Car- the Carpathian val leys. Studia Geomorphologica Carpatho- patho-Balcanica, 27–28: 29–44. Balcanica, 11: 33–51. Nilsen, T. H., 1985. Mod ern and an cient al lu vial fan de posits. Stupnicka E., 1963. Qua ter nary de posits in the Up per Vistula and Hutch in son Ross Bench mark, 87: 1–372, Van Nostrand So³a val leys, Carpathians. (In Pol ish, Eng lish summary ). Reinhold, New York. Biuletyn Geologiczny Uniwersytetu Warszawskiego, 3: 184– Rachocki, A. H. & Church, M. (eds), 1990. Al luvial Fans: A Field 262. Ap proach. Wiley, New York: 1–391. Szumañski, A., 1986. Late Gla cial evo lu tion and mech a nism of Robustelli, G., Muto, F., Scarciglia, F., Spina, V. & Critelli, S., trans for mation of a floor of the Lower San val ley. (In Pol ish, 2005. Eustatic and tec tonic con trol on Late Qua ter nary al lu - Eng lish sum mary). Kwartalnik AGH, Geologia, 12, 1: 5–92. vial fans along the Tyrrhenian Sea coast of Calabria (South It - Szumañski, A., 1986. Postglacjalna ewolucja i mechanizm trans- aly). Qua ter nary Sci ence Re views, 24: 2101–2119. formacji dna doliny Sanu. (In Pol ish). Kwartalnik AGH, Rose, J., 1995. Lateglacial and Early Holo cene river activ ity in Geologia, 12, 1: 1–92. low land Brit ain. In: Frenzel, B. (ed.), Eu ro pean River Ac tiv ity Vandenberghe, J., 2001. A typology of Pleis to cene cold-based and Cli matic Change Dur ing the Lateglacial and Early Ho lo - rivers. Qua ter nary In ter na tional, 79: 111–121. cene. ESF Pro ject “Eu ropean Paleoclimate and Man”, Spe - Vandenberghe, J., 2002. The re la tion be tween cli mate and river cial Is sue 9. Paläoklimaforschung/Palaeoclimate Re search, pro cesses, land forms and de pos its dur ing the Qua ter nary. 14: 51–74. Qua ter nary In ter na tional, 91: 17–23. Rust B.R., 1972. Struc ture and pro cesses in a braided river. Viseras, C., Calvache, M. L., Soria, J. M. & Fernandez, J., 2003. Sedimentology, 18: 221–245. Dif fer en tial fea tures of al lu vial fans con trolled by tec tonic or Schumm, S. A., 1977. The Fluvial System . Wiley, New York: eustatic accomodation space. Geo mor phol ogy, 50: 181–202. 1–338. White, K., Drake, N., Millington, A. & Stokes, S., 1996. Con - Smith, N. D., 1970. The braided stream depositional envi ron ment: strain ing the tim ing of al lu vial fan re sponse to Late Qua ter - compar i son of the Platte River with some Silu rian clastic nary cli ma tic Changes, south ern Tu ni sia. Geo mor phol ogy, rocks, north-cen tral Ap pa la chians. Geo log i cal So ci ety of 17: 295–304. Amer ica Bul le tin, 81: 2993–3014. Wil liams, P. F. & Rust B. R., 1969. The sedimentology of a Smith, N. D., 1972. Some sedimentological as pects of pla nar braided river. Jour nal of Sed i men tary Pe trol ogy, 39: 649– cross-strat i fi ca tion in a sandy braided river. Jour nal of Sed i - 679. men tary Pe trol ogy, 42, 624–634. Wójcik, A., Nawrocki, J. & Nita, M., 2004. Pleis to cene in the Sorriso-Valvo, M., Antronico, L. & Le Pera, E., 1998. Con trols on Koñczyce profile (Oœwiêcim Basin) – sedi ment gene sis and modern fan mor phol ogy in Calabria, South ern It aly. Geo mor - age anal y sis at the back ground of strati graphic schemes of the phol ogy, 24: 169–187. Qua ter nary. (In Pol ish, Eng lish sum mary). Biuletyn Pañstwo- Stanistreet, I. G. & Mc Car thy, T. S., 1993. The Okavango fan and wego Instytutu Geologicznego, 409: 5–50. the classi fi ca tion of subaerial fan sys tems. Sed i men tary Ge ol - Zieliñski, T., 1992. Moreny czo³owe Polski pó³nocno-wschodniej ogy, 85: 115–133. – osady i warunki sedymentacji. (In Pol ish). Uniwersytet Starkel, L., 1967. Wis³a wœród gór i wy¿yn. Przewodnik geolo- Œl¹ski, Katowice: 1–95. giczno-krajoznawczy. Z biegiem Wis³y, cz. I. (In Polish). Wydawnictwa Geologiczne, Warszawa.