sergey sedov, svetlana sycheva, victor targulian, teresa ... › articles › 62 › 44 › 2013 ›...

Last Interglacial paleosols with Argic horizons in Upper Austria and Central Russia – pedogenetic and paleoenvironmental inferences from comparison with the Holocene analogues

Sergey Sedov, Svetlana Sycheva, Victor Targulian, Teresa Pi, Jaime Díaz

How to cite: Sedov,S.,Sycheva,S.,Targulian,V.,Pi,T.,Díaz,J.(2013):LastInterglacialpaleosolswithArgichorizonsinUpperAustriaandCentralRussia–pedogeneticandpaleoenvironmentalinferencesfromcomparisonwiththeHoloceneanalogues.–E&GQuaternaryScienceJournal,62(1):44–58.DOI:10.3285/eg.62.1.05

Abstract: ThepaleosolsoftheLastInterglacialarepresentedinmanyloesssequencesoftheEuropeantemperatezonebysoilswithArgichorizon,thatareconsideredtobethepedologicalresponsetothebioclimaticconditionsofthatperiod.Westudiedmicromor-phological,physical/chemical(bulkchemicalcomposition,textureanddithionite-extractableiron)andmineralogicalcharacter-isticsoftwoprofiles–anEemianLuvisolinUpperAustria(Oberlaab)andaMikulinoAlbeluvisolinCentralRussia(AlexandrovQuarrynearKursk)tocomparethemwithrecentanalogoussoilsandtomakefurtherpaleoecologicalandchronologicalinfer-ences.Bothprofilesshowedasetofcharacteristics indicativeforweatheringofprimaryminerals,claytransformationillu-viationandsurfaceredoximorphic(stagnic)processes.PaleosolsdemonstratemoreadvanceddevelopmentthantheHoloceneanaloguesmanifestedhoweverindifferentpedogeneticcharacteristics.TheEemianLuvisolinUpperAustriaischaracterizedbystrongerclayilluviationmanifestedinhigherclaycontentandabundanceofilluvialclaypedofeaturesintheBthorizon.MikulinoAlbeluvisol inCentralRussia ismorestronglyaffectedbyeluvialandstagnicprocessesevidencedbydeeperandmoreintensiveaccumulationofbleachedsiltymaterialandclaydepletion.Wesupposethatthepropertiesofparentmaterialareresponsibleforthesedifferences.RussianAlbeluvisolisformedontheDneprloesspoorinweatherablemineralsandhav-inglimitedcapacityforbufferingacidityandclayformation.ThehigherdevelopmentstatusoftheLastInterglacialpaleosolscomparedtotheHolocenesoilshavinghoweversametypepedogenesisimplieslongersoilformationperiod,thatagreewithsomeofthepaleobotanicalproxiesandcouldincludebesidesMIS5epartofMIS5d;thewarmerandmoisterpaleoclimatedur-ingMIS5ecouldalsoaccountformoreadvancedpaleosoldevelopmentSeveralphasesofclayilluviationinterruptedbyfroststructuringanddeformationaredetectedintheEemianBthorizoninUpperAustria.ItsupposeevenlongerdevelopmentthatcouldextendtotheEarlyWürmianinterstadials(latesubstagesofMIS5)

Letztinterglaziale Paläoböden mit Bt-Horizonten in Oberösterreich und Zentral-Russland: pedogenetische und paläoum-weltbezogene Schlussfolgerungen im Vergleich mit den holozänen Analogen

Kurzfassung: InvielenLöss-Paläoboden-SequenzendergemäßigtenBreitenEuropasistdasletzteInterglazial(dt.:Eem,russ.:Mikulino)durcheinenBt-Horizont(ArgichorizonnachWRB)repräsentiert,deralspedologischesResultatentsprechenderbioklimatischerBe-dingungendieserZeitgedeutetwird.Wiruntersuchtenmikromorphologische,physikalische/chemische(Gesamtelementzusam-mensetzung,KorngrößenverteilungunddithionitlöslichesEisen)undmineralogischeCharakteristikaimProfilabschnittdesEem-LuvisolsinOberösterreich(Oberlaab)unddesMikulino-AlbeluvisolsinZentralrussland(AlexandrovGrubenaheKursk).AusdemVergleichderPaläobödenmitentsprechendenrezentenBödenergebensichpaläoökologischeundchronologischeSchlussfol-gerungen.BeideProfilezeigeneineReihevonCharakteristika,dieaufVerwitterungprimärerMineraleundTonmineralesowieTonverlagerungundredoximorpheProzessehinweisen.DiePaläobödenzeigenjeweilseineweiterfortgeschritteneEntwicklungimVergleichzuentsprechendenholozänenBöden,jedochanhandunterschiedlicherpedogenetischerMerkmale.DerEem-LuvisolinOberösterreichweisteinhöheresMaßanTonverlagerungauf,wasdurcheinenhöherenTongehaltundzahlreicheToncutaneimBt-Horizontgezeigtwird.DerMikulino-AlbeluvisolinZentralrusslandiststärkervonAuswaschungundStauwasserbetroffen,wassichintiefererundstärkererAnsammlungvongebleichtemschluffigemMaterialundTonverarmungzeigt.Wirnehmenan,dassdasAusgangsmaterialdieseunterschiedlicheEntwicklunghervorruft.DerrussischeAlbeluvisolbildetesichaufDnjepr-Löss,welcherimVergleichzudenRiss-LössenOberösterreichsärmeranleichtverwitterbarenMineralenistunddahereinegeringereKapazitätSäurezupuffernsowieTonneuzubildenaufweist.DasfortgeschrittenereEntwicklungsstadiumdesletztinterglazialenBodensimVergleichzuholozänenBöden,dieallgemeindemselbenBodentypentsprechen,sprichtfüreinelängereBodenentwick-lungsphase,wasmitpaläobotanischenErgebnisseninEinklangsteht.EinerseitskönntederletztinterglazialePaläobodennebendemMIS5eauchTeiledesMIS5dumfassen,andererseitskönnteeineintensiverePaläobodenentwicklungdurchdaswärmereundfeuchterePaläoklimawährendderInterglazialphasedesMIS5everursachtwerden.MehrerePhasenderTonverlagerung,unterbro-chendurchfrostdynamischeStrukturierungundDeformationsindimeemzeitlichenBt-HorizontinOberösterreichnachweisbar.DienochweiterreichendeEntwicklungkönntebisinnochjüngereFrühwürm-Interstadialegereichthaben.

Keywords: Last Interglacial, paleosol, Argic horizon, paleoclimate

Adresses of authors: S.Sedov*,T.Pi,J.Díaz,InstitutodeGeología,UNAM.CircuitodelaInvestigaciónCientífica,04510,MéxicoDF,Mexico;S.Sycheva,V.Targulian,InstituteofGeography,RAS.Staromonetny29,Moscow,119017.Russia;*corresponding author:[email protected]

44 E&G / Vol. 62 / No. 1 / 2013 / 44–58 / DOI 10.3285/eg.61.2.05 / © Authors / Creative Commons Attribution License

E&G Quaternary Science Journal Volume 62 / Number 1 / 2013 / 44–58 / DOI 10.3285/eg.62.1.05www.quaternary-science.net GEOZON SCIENCE MEDIAISSN 0424-7116

http://www.quaternary-science.net

45E&G / Vol. 62 / No. 1 / 2013 / 44–58 / DOI 10.3285/eg.61.2.05 / © Authors / Creative Commons Attribution License

1 Introduction

Theperspectiveofglobalclimatechangeincreasedtheinter-esttothepaleoecologyofearlierwarmerperiods,inpar-ticulartotheQuaternaryinterglacials.Thelastinterglacial(knownintheregionalstratigraphiesasRiss-Würm,Eemi-an,Mikulino,Sangamonian)drewspecialattentionasfarasthecorrespondinggeologicalobjectsandmaterialsarefrequentandwellpreserved.Duringthelastdecadesasig-nificantprogresswasachievedindefiningthedurationofthiswarmphaseanditspaleoenvironmentalcharacteristicsbasedon thecorrelationsbetweenmarineand terrestrialrecords(Shackletonetal.2003;Sieretal.2011).

Paleosols of loess-paleosol sequences are among themostimportantterrestrialrecordsofinterglacialenviron-ments, especially since these sequences were thoroughlycorrelatedwiththedeepseaisotoperecord(Kukla1977;Brongeretal.1998).Inthecontemporarytemperatezoneof Europe the paleosols of the last interglacial are oftenrepresented by soil bodies with strong clay illuviation(Haesaerts&Mestdagh2000),whichwereconsideredtobe,withcertainlimitations,themostsignificantresponseof pedogenesis to the interglacial bioclimatic conditions(Stephan 2000). The examples are the Ipswichain paleo-argillic soils in England (Catt 1996), Rocourt Luvisol inFrance (Antoineetal.1999)andBelgium(Haesaertsetal.1999;Vandenhauteetal.2003;Vancampenhoutetal.2008),ErbacherBoden–Luvisol/Alfisol/ParabraunerdeinGermany(Mahaneyetal.1993;Antoineetal.2001;Ter-horstetal.2001),lowerLuvisolofthePK3pedocomplexinCzechia(Demek&Kukla1969;Frechenetal.1999)andNietuliskoI-GJ1pedocomplexinPoland(Jary2009,2011),“brown-podzolic soil” of Pryluky-Kaydaky pedocomplexinUkraine(Rousseauetal.2001;Gerasimenko2006)andSalynpaleosol,theLuvisolofMezinpedocomplexinCen-tralRussia(Velichko1990;Yakimenko1995;Velichkoetal.2006).

Onlyinareaswithdriercontinentalclimatethelastinter-glacialpaleosolsdonotshowclayilluviation:inLowerAus-

tria(Fink1956;Bronger1976;Peticzka2009;Sprafkeetal.2013,thisvolume)itisrepresentedbyCambisols,whereasinthesouth-easternpartoftheEastEuropeanPlain(Rutteretal.2003)andtheCarpatianBasin(Bronger1976;Marko-vicetal.2008)thelastinterglacialsoilscorrespondtoCher-nozems.Infact,intheEuropeantemperatezoneLuvisolsoccupiedalargerarealintheEemiansoilcoverthantheydointheHolocene.

Thisareadiffersespecially in theEastEuropeanPlainwhere the zone of forest soils was much broader duringtheEemianandoccupiedalargeportionofthepresentdaysteppezone(Morozova1981;Morozovaetal.1998).InanumberofsitesinCentralRussianandUkrainiansteppere-gionsonecanseeastrikingdifferencebetweenHoloceneChernozemonthesurfaceandburiedMikulinoLuvisol,sep-aratedbyValdayloess,allexposedinthesamecut(thisisalsothecaseinAlexandrovquarryexposure).

In thepresentday temperatehumid forestareasboth,last interglacialandHolocenesoilsshowclay illuviation.However,theyareoftenclearlydistinguishedquantitatively:strongerdevelopmentofthelastinterglacialArgichorizonscomparedtotherecentoneswasreportedinanumberofcasestudies(Boardmann1985;Bullock&Thompson1985;Mahaneyetal.1993).Thereasonsforthisdistinctionarenotsoobvious:differencesinbioclimaticconditionsaswellasindurationofpedogenesiscouldbeinvolved.

Wehavetoconcludethatbothpaleoecologicalandchron-ologicalaspectsofthelastinterglacialLuvisolsdevelopmentarefarfrombeingclear.Concerningthepaleoenvironmen-talsettingtheassumptionthattheBthorizonisareliablesignofinterglacialconditions“definedbythereturnofthetemperatedeciduouswoods”(Stephan2000)couldbetooambitious:weknowthatinthepresentdaysoilcoverthesehorizonsoccurinamuchbroaderspectrumofecosystems.IntheclassiczonalsequenceoftheEasternEuropesoilswithstrongclayilluviationareformedonloamysubstratesfromthebroadleafforestsandforest-steppetillborealconiferousnortherntaiga(Gerosimovaetal.1996).InfactwithintheEurasianforestbeltonlyintheregionswithdrierextra-con-tinentalclimateandpermafrostinMiddleandEasternSi-beriaclayilluviationishampered(Gerosimovaetal.1996).

BroadecologicallimitsoftherecentArgichorizonforma-tionhaveimplicationsfordeterminingitstiminginEurope.In the courseof soil evolutionduringandafterLastLateGlacial,clayilluviationisdetectednotonlyintheHolocenebutalsointhelateMIS2interstadials(Kühn2003).SomeauthorsattributethedevelopmentofArgichorizonsintheEuropeanLuvisolsmostlytothelateglacial(Bølling)bo-realpaleoenvironment(vanVlietLanoë1990).

Thus the possibility should be considered that also inMikulino/Eemian paleosols the Luvisol pedogenesis oc-currednotonlyduringtheinterglacialsensustrictobutalsointransitionalphasesofcolderforestorforest-steppeeco-systemsbeforeandafterit.Infact,thisscenariohasbeenalreadyproposedbyvariousresearcherswhodetectedsev-eralclayilluviationphasesintheEemiantoEarlyWurmi-anpedocomplexesinBelgium(Haesaertsetal.1999;Hae-saerts&Mestdagh2000)andGermany(Antoineetal.2001;Terhorstetal.2001).AlltheseauthorscoincidedindiscriminatingbetweenforestLuvisoldevelopmentcorre-spondingtothewarmhumidinterglacialandforest-steppe

Fig. 1: Geographical situation of the studied profiles. O – Oberlaab, A – Alexandrov.

Abb. 1: Geographische Lage der untersuchten Profile. O – Oberlaab,

A – Alexandrov.


GreyForestSoilsattributedtocoolercontinentalclimateoftheEarlyWeichselianinterstadials.ThisapproachrevivestheearlierideasofBoardmann(1985)aboutlongerpedo-genesisofthePleistoceneinterglacialpaleosolscomparedtotheHolocene.

However,inmostworksonloessstratigraphy,chronologyandpaleoecologytheinformationonpaleosolpedogenesisisratherlimited:theconclusionsaremostlybasedonfieldmorphologicalobservations,grainsizeandmagneticsuscep-tibilitydistribution.Deeperunderstandingofpaleoenviron-mentalsignificanceofthepaleosolofthelastinterglacialinEuroperequiresmoredetaileddataaboutthetypesandsuc-cessionofpedogeneticprocesses–whichcanbeprovidedbydetailedmicromorphologicalandclaymineralogicalinves-tigationaccompaniedbysoilchemicalanalyses(Bronger1976;Bronger&Heinkele1990;Kemp1999).

SuchdetailedstudyoftheburiedLuvisolspromisetobeeffectivealsoconcerningtheircomparisonwithmodernsur-facesoils.Temperateforestsoilswithclayilluviationareprovidedwithoneofthemostvariableanddetaileddata-setsofmorphological,physical/chemicalandmineralogicalcharacteristics.Infact,thesesoilswereoneofthemain“ex-perimentalpolygons”ofpedologytorconstructscenariosofpedogenesis(includingpolygeneticmodels)basedonthesecomplexdatasets(e.g.Targulianetal.1974a,b;Kühnet

al.2006).Thus,theactualisticapproachtowardspaleosolin-terpretationwasexpectedtobemostfruitfulincaseoftheLuvisols.

ThisresearchintendstocontributetotheknowledgeaboutthelastinterglacialsoilevolutioninEuropebycarryingoutacomparativepedogeneticanalysisoftwoburiedpaleosolswithArgichorizonformedonloessingeographicallydistantandecologicallydissimilarregions:UpperAustria(Oberlaabsection)andCentralEuropeanRussia(AlexandrovquarrysectionnearKursk).Thefinalobjectiveistodevelopsce-nariosofpaleosolgenesisandevolutionforbothprofilesandfromthisderiveconclusionsabouttheirpaleoenvironmentalsignificanceandtiming.

2 Materials and methods

Twoprofilesofthelastinterglacialpaleosolsfromtheloess-paleosolsequencesweresubjectedtodetailedmorphologi-calanalysisandsamplingbeingselectedasthekeysitesfortheICSU-2003project“PolygeneticmodelsforPleistocenepaleosols”(Fig.1).TheprofileinOberlaab(UpperAustria)islocatedonthefluvioglacialterraceattributedtotheMindelglaciation,closetoitsbench(Terhorst2013,thisvolume).ThepresentdayclimateishumidprovidingconditionsforbroadleafforestvegetationandforadevelopmentofStag-nicLuvisolsasdominantmodernsoiltype.TheprofileAl-exandrovquarry(nearKursk,CentralRussianPlain)islo-catedatthewatershedpositionclosetotheslopetowardsthevalleyofriverMlodat.Themodernclimateistemper-ate semi-humid, the surface soils are Haplic Chernozemsformedundermeadow-steppevegetation.Thus,bothstudysitespresenttwomajorcasesofinterrelationbetweenlastinterglacialLuvisolsandtheHolocenesoil:theybelongtothesametypeincaseofOberlaabandtheyaregeneticallydissimilarincaseofAlexandrovsection.

Thestratigraphic,chronological,andpaleoecologicalas-pects of both paleosol-sedimentary sequences were pub-lishedearlier.ForOberlaabthesedataareavailableinthepapersincludedinthisSpecialVolumeandsomeearlierpub-lications(Terhorst2007,2013,thisvolume;Solleiroetal.2013,thisvolume).TheEemiansoilinOberlaabistheupper-mostof5buriedpaleosols;itisseparatedfromthemodernsoilbycolluvialandloessicsedimentswithsignsofweakpedogenesis,attributedtotheWürmianglacial.AlexandrovsectionwasstudiedbySychevaandco-authorsduringthelast20years,theresultsarepresentedinseveralpapers(c.f.Sycheva1998;Golyeva&Sycheva2010;Sycheva&Sedov2012).Mikulino(Salyn)paleosolisdevelopedontheDnieper(RissianGlacial,MIS6)calcareousloess.Theimportantad-vantageofAlexandrovsectionisanextensiveanddetailedpartcorrespondingtothelast(Valday)glaciation,overlyingtheMikulinosoil.Thelowersegmentofthispartiscom-prisedbythreeEarlyValdaypaleosolsclearlyseparatedbycolluvialstrata.AbovethemtheMiddleValdaypaleosolisdeveloped(Bryansksoil).Finally,modernChernozemissep-aratedfromBryansksoilbytheLateValdayloess.

Detailed morphological description of the last inter-glacialpaleosolprofileswas followedbysamplingof thegenetichorizons:bulksamplesforphysical,chemicalandmineralogicalcharacteristicsandblockswithundisturbedstructure for thin sections were collected.Micromorpho-

Fig. 2: Profile morphology of the Eemian paleosol of the Oberlaab profile, with the overlying Würmian pedosediment (WP).

Abb. 2: Eemzeitlicher Paläoboden im Profil Oberlaab mit darüber liegen-dem würmzeitlichem Bodensediment.


logical observations were performed under petrographicmicroscopeandthedescriptionsfollowedtheterminologyofBullocketal.(1986).Wegavespecialattentiontothepedofeaturesrelatedtotheclayeluvial-illuvialredistribu-tion, redoximorphicprocessesaswellas the signsofag-gregation and mixing by biotic and cryogenic processes.The properties selected for paleosol laboratory analyseswerethoseindicativeofancientpedogeneticprocessesandnotsubjectedtomajordiageneticchangesafterburial.BulkchemicalcompositionwasestimatedbyX-rayfluorescenceanalysis.Grainsizedistribution–intendedtoestimateclayaccumulationduetoweatheringandilluviation–includedseparationofsandfractionsbysievingandquantificationofsiltandclaybypipettemethod.Thecontentoffreeironoxides – an important product of soil weathering – wasevaluatedbymeasuringFeinthedithionite-citrate-bicar-bonateextract(Fed).Claymineralassemblagesinthesoilswitheluvial-illuvialdifferentiationareknowntobespecif-icfordifferenthorizonsandstronglyinfluencedbypedog-eneticprocesses(Targulianetal.1974b;Tonkonogovetal.1987).WestudiedthecompositionofclayfractionbyX-raydiffractionusingaShimadzuXRD-6000diffractometerinorientedspecimensubjectedtodifferentpretreatments:air-dry,saturatedwithethylene-glycol,heatedto375 °cand500 °c.Clayspeciescontentwasestimatedinsemi-quanti-tatively,usingsimplepeakweightingfactors;forareaesti-mationweusedFityk(Wojdyr2010)program.Illite,smec-titeandmixed-layeredcomponentswereidentifiedbysep-aratingtheirpeakareas in theglycolatedXRD-traceandcalculatingtheirproportions(Moore&Reynolds1997).

Allresultswerefurtherintegratedwithotherdatasets–morphological,geochemical,rockmagnetic,etc.publishedforOberlaabbySolleiroetal.(2013,thisvolume),forKurskbySycheva(1998),Rivasetal.(2003)andSycheva&Sedov(2012).

Thekeyelementofinterpretationconsistedinthecom-parison of obtained results with the existing knowledgeaboutthepedogeneticcharacteristicsoftheclay-illuvialsoilsformedunderdifferentenvironmentalconditions:temperateforestofWesternandCentralEurope(Jamagneetal.1984;Kühnetal2006;Saueretal.2009),taiga(Targulianetal.1974a,b;Tonkonogovetal.1987)andforest-steppe(Mie-demaetal.1999)ecosystemsofEuropeanRussia.Referenceprofiles for comparison were modern analogues (surfacesoils)ascloseaspossibletotherespectivestudiedprofileforwhichthenecessarypedogeneticcharacteristicswereareavailable:surfaceHoloceneLuvisolforOberlaab(Solleiroetal.2013,thisvolume)andmodernAlbeluvisoloftheMos-cowregion(Targulianetal.1974a,b).

3 Results

Paleosol morphology from macro- to microscaleTheEemiansoilinOberlaabislocatedatadepthofabout3mbelowtheHoloceneLuvisol,formedonWürmiansedi-ments.Thelowerpart(60cm)ofthelatterdirectlyaboveEemian Bt horizon has yellow color, silty loam textureand contains ferruginous concretions. This morphologytogether with gradual wavy boundary suggests that thislayercouldbeapedosedimentthatincorporatedmaterialoftheEemianeluvialhorizon(indicatedinthetablesand

figuresasWP–Würmianpedosediment).Theunderlying90cmthickbrownBtghorizon(subdividedintoBtg1andBtg2) isdarker,more compact and clayey than theover-lying pedosediment, with platy/subangular blocky struc-ture.Brownclaycoatingscoverpedsurfacesandfillverti-calcracks.Furthermore,fewpalecoatingsofbleachedsilt,ironconcretionsandmottlesarepresent.Clayilluvialfea-turesdecrease in theunderlyingBCtgandBCghorizons(jointthicknessabout1m),wherelargervisiblecutansarerestrictedtoveryfewbiogenicpores–channelsandcham-bers.Simultaneously,stagniccolourpatternappears–paleareas,oftenofsubhorizontallenticularshapeareneighbor-ingwithyellowmottlesofferruginouspigment.Belowfol-lowsthepalebrown-yellowhomogeneousChorizon–theloessicsedimentofRissglaciationsseparatingtheEemianprofile from the underlying Middle Pleistocene paleosol(Terhorst 2007; Solleiro et al. 2013, this volume). Thesoilwasclassified in thefieldasStagnicCutanicLuvisol(Fig.2).Underthemicroscope,thegroundmassinallho-rizons is dominated by coarse silt, having rich and vari-able mineralogical composition: besides quartz feldspars,amphibolesandmicasareabundant.Micasarerepresentedbothbycolorlessmuscoviteanddarkbrownbiotite;inthelatteratstrongermagnificationsignsofweatheringareob-served–weakinterferencecolorsandpleochroism,defor-mation,precipitationofironoxides.

The Würmian y0pedosediment (WP) has areas withbandedfabricdemonstratingstripesofcoarsesiltandfinematerial. Frequent ferruginousnodules– rounded, circu-lar,compoundaredistributedwithinthegroundmass,fewthin clay coatings are present. Areas with banded struc-turewerealsoobservedintheBtg1horizon.Clayilluvialpedofeaturesbecomemoreabundantinthishorizon,beingpresentedbothbyundisturbedclaycoatings(mostlythinandimpure)(Fig.3a)intheporesandfragmentedandde-formedclustersofilluvialclayincorporatedintoground-mass. Ferruginous nodules and mottles, mostly with ir-regular shape and diffuse boundaries are also abundant.Ratherbiganorthiciron-claynodulesofsubangularfrag-mentedshape(Fig.3b)andcharcoalfragmentswiththetis-suestructureofaconifertreewereencountered.

Themajorabundanceandvarietyofclayilluvialmateri-alswasfoundintheBtg2horizon.Undisturbedclaycoat-ings are present, however, they are not dominant. Frag-ments of clay illuvial pedofeatures of different size andmorphology are more frequent, some of them are largerthananyoftheundisturbedcoatings(Fig.3c).TheBtg2ho-rizon is characterized by strong fracturing giving rise toangularblockyandcoarselenticularpeds(Fig.3d)andbe-ing accompanied by displacement along the cracks. Thewalls of these cracks support thin undisturbed coatings.Bleached irregular shaped silt concentrationsdepletedofclay are very rare (Fig. 3e). Few infillings with bow-likestructureareofzoogenicorigin(Fig.3f)(Kooistra&Pul-leman2010).

DeeperintheBCtghorizonthenumberofclayilluvialpedofeaturesdecreasesbuttheirpreservationincreases–theyaremostlyundisturbedcoatingsinvoids,someofthemlargeandlaminated(alternatinglimpidwithstronginter-ferencecolorsandimpuremicrolayers)(Fig.3g,h).FurtherdowntheprofileintheBCghorizonclaycoatingsareeven


a) Impure clay coatings, Btg1 horizon, plain polarized light.

b) Anorthic ferruginous nodule, Btg1 horizon, plain polarized light.

c) Fragment of clay illuvial pedofeature, note strong interference colors and microlamination. Btg2 horizon, crossed polarizers.

d) Angular blocky – lenticular structure produced by fracturing; note thin clay coatings on the aggregate surface. Btg2 horizon, plain polarized light.

e) Concentration of bleached silt particles. Btg2 horizon, plain polarized light.

f) Infilling with bow-shaped structure. Btg2 horizon, plain polarized light.

Fig. 3: Micromorphology of the Eemian paleosol in Oberlaab.

Abb. 3: Mikromorphologie des eemzeitlichen Paläobodens in Oberlaab.


g) Laminated clay coatings with limpid and impure microlayers. BCtg horizon, plain polarized light.

h) Same as g), crossed polarizers; note high birefringence of limpid layers.

i) Clay illuvial pedofeature with ferruginous coatings on the surface and in the cracks. BCg horizon, plain polarized light.

j) Bleached area in the groundmass under clay coating. BCg horizon, plain polarized light.

k) Disturbed clay illuvial pedofeature, fragments covered by a thin undis-turbed clay coating. BCg horizon, plain polarized light.

l) Parallel orientation of elongated mineral particles, C horizon, plain polarized light.


fewerandusuallycombinedwithferruginousnodulesandfilmspenetratingintoilluvialclay(Fig.3i).Frequently,claycoatingsintheporesoverlybleachedmicroareasadjacenttotheporewalls,however,theseareasalthoughlackingfer-ruginouspigmentarenotdepletedoffineclaymaterial(Fig.3j).IntheBChorizonsfewclaypedofeaturesarefragmentedbutusuallynotincorporatedintogroundmass–thefrag-mentsstayintheporesbeingonlyslightlydisplacedandcoveredbythenewgenerationofthinnercutans(Fig.3k).FinallyintheChorizonallpedofeaturesbecomelessabun-dantandprimarysedimentarystructuresaremoreevident–amongthemparallelsubhorizontalorientationoftheelon-gatedmineralparticles(Fig.3l)

The profile of Mikulino paleosol as mentioned aboveisoverlainby6mofWaldaysedimentswithaHoloceneChernozemontop.Theprofiledemonstratesaremarkablepreservationofallhorizonsincludingthetopsoil.Itisde-limited from theoverlying laminated colluvial sedimentsbyathin(lessthan1cm)blacklayerofburnedlitter.Be-low it a grey-brown Ah horizon (8 cm thick) is located;itcontainsnumerouscharcoalparticles(havingtendencytoparallelorientation)and fewsoft ferruginousnodules,sometimesassociatedwiththecharcoal.Itisunderlainbytheverypale20cmthickEhorizonwithwell-developedmulti-order platy structure. Iron oxide nodules (soft andhard)becomemoreabundant,whereascharcoalparticlesare fewer.An importantdiagnostic feature is the typeofthelowerboundaryofthishorizon.Itisgradualwiththebleached material penetrating into the underlying layeralongporesandfissuresanditformsthinglossicfillsintheverticalcracks–knownas“albeluvictonguing”.Thedown-ward“invasion”ofbleachedsiltmaterialdefinesthe15cmthick transitional EB horizon. It still has platy structure,however,platyaggregatesarethickerandbreakintosmallsubangularblocks.Thebleachedmaterialconcentratesontheaggregatesurfacewhereas the internalpart isdarkerandcontainsmoreclay.Thisdistributionproducesaheter-ogeneouscolorpattern:thenetworkofpaleveinsisspreadamongthebrown“islands”.Iron-manganesepedofeatures

arepresentedbysmallnodulesandfilmsmostlyassociatedwiththethinfissures.

Theilluvialpartoftheprofile(Bt1,30cmthick–Bt2,35cmthick–Bt3,65cmthick)ismarkedbyacontrastingdif-ferenceofmainmorphologicalcharacteristics.Ithasclayeyloamytexture,subangularblockytoprismaticstructureandpredominantlybrowncolor.However,siltybleachedmate-rial is still abundant: in theBt1horizon it formsfilmsonmostpedsurfaces.Inmanycasesthesefilmsoverlybrownclaycoatings.InBt2thepalesiltcomponentdecreasesandisrestrictedmostlytothelargerverticalcracks.Aggregatesare covered with continuous clay coatings. The prismaticblockypedsbecomecoarserandclaycoatingsontheirsur-facesturnpatchyintheBt3horizon.AllArgichorizonshavealsoferruginouspedofeatures,inBt1thesearemostlysmallnodules,whereasinBt2andBt3dendriticiron-manganesespotsoccur.

TheBChorizonshavebrighterbrown-yellowcolorandweaker pedogenic structure. Where the paleosol lies onDnieperloessweobservedaclearbandedpatterninthesehorizons:darkerclayeystripeswerealternatingwith thepale-yellowsiltybands.

Allthesehorizonsarefreeofcarbonatesandthelatterappearonlyintheunderlyingloess,atthedepthof250cmfromtheMikulinosurface.ThepaleosolwasdefinedasHap-licAlbeluvisol(Fig.4).

Microscopic observations reveal predominance of siltgrainsinthegroundmass.Theirmineralogicalcompositionisratherpoor–quartzisclearlydominant,K-Nafeldsparsarepresentinminorquantities,micasandheavymineralsarefew.

TheAhorizonhascomplexmicrostructurewithcombina-tionofplatyandisometriccrumbyaggregates.Darkorganicpigmentwithheterogeneousdistributioncausesinterchang-ingofdark-coloredandlight-coloredmicro-zones.Therearefewsignsoffaunalactivity:somezoogenicchannelswithexcrementinfillingswerefound;groundmasscontainsnu-merouscharcoalparticles(Fig.5a).

IntheEhorizondominantfineplatyaggregatesdemon-stratecleartexturaldifferentiationwithprevailingbleachedcoarsesiltintheupperpartsandclosetotheporesandfinesiltandplasmicmaterialinthecentralandlowerparts.Fre-quentcompactroundedsimpleironnodulesarewidespreadinthegroundmass,sometimescharcoalisobservedintheirnucleus(Fig.5b).Weencounteredfragmentsofclaycoatingsembeddedinthebleachedsiltymatrix(Fig.5c,d).

TheEВhorizonalsohaswelldevelopedplatystructurewithevenstrongerintra-pedaldifferentiationofparticlesize.Finesiltandclayisconcentratedinsidetheplates,whiletheperiphericalpartsconsistofbleachedsilt.Ironpedofeaturesarefrequentandvariable:weobservedroundednodulesandincrustationofplatyaggregatesmainlyonthebottomside(fig.5e).

TracesofplatyaggregationarestillobservedintheBt1horizonbutplatesarefrequentlyneighbouringsubangularblocks(Fig.5f).Theporeshavecommonbleachedsiltycoat-ingsaswellasinfillings,whereasdeformedandfragmentedilluviatedclaypedofeatureswerefoundintheinteriorofthepeds(Fig.5g).Undisturbedclayilluvialpedofeaturesstillre-latedtotheporeswerenotobserved.Smallferruginousnod-ulesarefoundboth,inthegroundmassandsiltyinfillings.

Fig. 4: Profile morphology of the Mikulino paleosol in Alexandrov: position in the sequence, eluvial-illuvial differentiation, detail of the Bt1 morphol-ogy, showing bleached areas related to the pores.

Abb. 4: Morphologie des Mikulino Paläobodens in Alexandrov: Lage im Profil, Differenzierung von Eluvial- und Illuvialbereichen, Detailaufnahme Bt1-Horizont mit gebleichten Bereichen, die im Zusammenhang mit Poren stehen.


OnlytheВt2andВt3horizonshaveundisturbedlayeredilluvialclaycoatingsontheporewalls(Fig.5h).However,bleachedsiltconcentrationsarestillpresentandconcentrat-edmainlyinfissuresandlargechannels.Theyhaveabruptboundariestothegroundmass,andsometimestheyarejux-taposedontheclaycoatingsoroccur intheneighboringpores(Fig.5i,j).

InthethinsectionsofthebandedBChorizonsweob-servedaclearlaminarstructurewithalternatingbandsen-richedincoarsesiltandfineclaymaterials.Eveninthesehorizonsweobservedfewthinclaycoatings,whichshowednoclearpreferenceforspecificbands.

Physical and chemical characteristicsBulkchemicalcompositiondemonstratessimilartendenciesofprofiledifferentiationintermsofelementconcentrations.TheuppereluvialhorizonshavehigherquantitiesofSiattheexpenseofAlandalsoFeandMg.However,itshouldbenotedthatabsolutevaluesarequitedifferentinthetwostudiedprofiles:thematerialofMikulinopaleosolinAlex-androvhasmuchhigherSicontent(80–85%)thanthatoftheEemiansoilinOberlaab(70–76%),whereasthelatterismorerichinAl,Feaswellasalkalineandalkalineearths(exceptKthathassimilarconcentrationsinbothpaleosols)(Tab.1).

Clay content shows a clear and similar distributiontrendinbothprofiles:themaximumisobservedintheBthorizons,whereaslowervaluesarefoundintheeluvialEhorizoninAlexandrovandupperWürmianpedosedimentinOberlaab (in the latter–with contrastingfluctuationsbetweenupperandlowerparts).Thehighestvaluesofthedithionite extractable ironalso correspond to the illuvialpartofbothprofiles.However,ironandclaymaximadonotcoincide:ironcontentishighestintheupperBt1horizons,

whereasclayhasitsmaximumbelowintheBt2horizons.Again, both clay and Fed contents although having verysimilar distribution tendencies in both profiles, demon-stratedifferentabsolutevalues.ForbothcomponentstheyareconsiderablyhigherintheOberlaabprofile(Tab.2).

Claymineral assemblages showverycleardifferentia-tion in both studied profiles. Interlayered illite-smectitewithvariableproportionofbothcomponents–(1.4–1.5nmpeak,shiftingtosmalleranglesonglycolation)decreasesstronglyintheeluvialEhorizonsandismuchhigherintheilluvialstratumandparentmaterial. In theEemianLuvi-solofOberlaabthistendencyisratherweakandexpressedmostlyindifferentproportionsofsmectite-richandsmec-tite-poormixedlayeredcomponents.Thelatterincreaseintheupperpartoftheprofile. IntheMikulinoAlbeluvisolof Alexandrov this tendency is much stronger: all smec-titiccomponentsdecreaseintheeluvialpart,whereasonthecontrary, illiteandkaolinite (respectively1.0nmand0.7nmpeak,thelatterdisappearingafter550°cheating)aremoreabundant(seeTable3andFig.6).Onlyinthepedo-sediments,eluvialandupperilluvialhorizons(EBandBt1)we found mixed-layered minerals with chloritic compo-nent(“shoulder”of1.0nmpeaktowardssmalleranglesaf-terheatingindicatingincompletecontractionof1.4–1.5nmmaximum),whichweidentifywiththehydroxyl-interlay-eredvermiculiteandsmectite(HIVandHIS)(Bamhisel&Bertsch1989).

4 Discussion

Pedogenesis of paleosols – comparison with the region-al modern analoguesThequestiontobeansweredbeforesoilformingprocessesinthepaleosolcanbeassessedishowcompleteistheirprofile

HorizonTotal element concentrations, %

SiO2 TiO2 Al2O3 Fe2O3 MgO CaO Na2O K2O

Eemian paleosol (Oberlaab, Austria)

WP upper 74.14 1.12 14.86 4.95 1.03 0.81 0.97 1.94

WP lower 74.46 1.12 14.75 4.68 1.01 0.85 1.00 1.92

Btg1 76.16 1.03 13.15 4.66 1.09 0.66 0.94 2.11

Btg2 70.26 0.94 16.49 6.38 1.60 0.67 0.79 2.60

BCtg 70.58 0.95 16.02 6.30 1.63 0.81 0.88 2.58

BCg 71.37 0.94 15.33 6.01 1.59 0.91 1.04 2.56

C 71.48 0.96 15.47 5.86 1.55 0.93 1.03 2.45

Mikulino paleosol (Alexandrov quarry, Russia)

A 82.30 0.90 9.44 2.68 0.61 0.81 0.65 2.34

E upper 85.37 0.90 7.69 1.88 0.43 0.62 0.56 2.38

E lower 83.72 0.94 8.54 2.33 0.55 0.58 0.64 2.52

EBt 81.97 0.95 9.30 3.14 0.71 0.60 0.58 2.62

Bt1 81.30 0.92 9.70 3.40 0.73 0.62 0.55 2.63

Bt2 81.01 0.81 10.23 3.44 0.78 0.64 0.53 2.37

Bt3 80.67 0.79 10.49 3.45 0.76 0.67 0.59 2.39

BC 82.17 0.77 9.60 3.02 0.64 0.68 0.49 2.43

WP – Würmian pedosediment

Tab. 1: Bulk chemical composition: selected major elements .

Tab. 1: Ergebnisse der Elementaranalysen: Aus-gewählte Hauptelemente.


a) Pore with the excremental infilling, charcoal particle. A horizon, plain polarized light.

b) Ferruginous nodule with charcoal in the center. E horizon, plain polarized light.

c) Fragment of clay coating surrounded by bleached silt. E horizon, plain polarized light.

d) Same as c), crossed polarizers; note strong interference colors and undu-lating pattern of extinction.

e) Platy structure, fissures between the plates are filled with bleached silt, ferruginous hypocoatings are located on the lower surfaces of the plates. EBt horizon, plain polarized light.

f) Platy and blocky aggregates, pores are filled with bleached silt, intra-pedal matrix enriched with fine material. Bt1 horizon, plain polarized light.

Fig. 5: Micromorphology of the Mikulino paleosol in Alexandrov.Abb. 5: Mikromorphologie des Mikulino Paläobodens in Alexandrov.


andtowhatextenditisaffectedbypost-burial(diagenetic)processes.

IntheOberlaabprofilethelayerdirectlyabovetheEemi-anBthorizonhasclearsignsofsedimentationandmixing.Thesesignsarestrongerintheupperpartofthishorizon,wheregrainsizefluctuationsmarkalithologicaldiscontinu-ity;inthislayerfewthinclaycoatingsaremostprobablythelowermosttracesofclayilluviationfromtheHoloceneLuvi-sol.However,stagnicferruginouspedofeaturesandpresenceofthespecificclaycomponent–hydroxylinterlayeredver-miculitesandsmectitessuggestthatmaterialoftheeluvialhorizon,althoughredepositedispresentinthislayer.Minorsignsofdisturbance(anorthiciron-claynodules,charcoal)arepresentevenintheBt1horizon,andthepaleosolissup-posedtobeintactonlybelowtheBt1(Terhorstetal.2003).

IncaseofAlexandrovquarrythegradeofpreservationishigh:acompletesequenceofgenetichorizonsincludingtheburnedlitterispresent.OnlytheAhorizonhassignsofre-deposition:orientedcharcoalparticles.Moreover,noeffectsofposteriorpedogenesisaredetectedinthispaleosol,duetoitsprotectionbyathickoverlyingsedimentlayer.

Inbothprofilesasimilarsetofpedogeneticprocessesisdetected.Clayilluviationisevidencedbyclaycoatings(ob-servedbothonmacro-andmicroscale)aswellasamaxi-mumofclaycontentintheBthorizoncomparedbothtotheunderlyingCandoverlyingEhorizon(insituorredepos-

ited).Clearmicromorphologicalsignsofsilicateweatheringareobservedinthebiotiteparticles.Increaseofdithioniteextractableiron,whichmostlyincludesfineoxidesproducedbyweatheringisanimportantanalyticalindicator.Anen-hancedSicontentintheeluvialhorizonsofLuvisolsisofteninterpretedasaresultofdecayofallunstablesilicates(in-cludingpartofclayminerals)andresidualaccumulationofquartz(Targulianetal.1974b).Lossofsmectitesinthesamehorizonsisalsoconsideredtobearesultofselectivedestruc-tionofthemostunstableclaycomponents(Tonkonogovetal.1987).However,itshouldbetakenintoaccountthatclayilluviationcouldalsocontributetotheseproperties.RemovalofclayfromEhorizonalsocouldcauseanincreaseofSi,duetorelativeaccumulationofcoarsecomponentsricherinthiselement.Smectitesaremostfineanddispersablecompo-nents,thatcouldbepreferentiallymobilizedbysuspensiontransportandremovedfromtheeluvialhorizons(vanRanstetal.1982).Thus,geochemicalandmineralogicalindicatorsgiveamixedsignalfrombothprocesses,afactthatunfor-tunatelyisrarelytakenintoaccountwhenelementalcom-positionofloess-paleosolsequencesisinterpretedthroughvarious“weatheringindices”.

More clear evidence of clay mineral transformationisprovidedbytheHIVaccumulationintheupperpartofthepaleosols.Thiscomponentisknowntobeformedfrom2:1claymineralswithlabilestructureduetosynthesisof

g) Fragmented and deformed clay illuvial pedofeatures incorporated into groundmass. Bt1 horizon, plain polarized light.

h) Continuous undisturbed clay coating in the pore. Bt3 horizon, plain polarized light.

i) Bleached silt (left) and limpid clay coating (right) in the neighboring pores. Bt3 horizon, plain polarized light.

j) Same as i), crossed polarizers, note strong interference colors of the clay coating.


fragmentaryAl-hydroxyllayerbetweenthe2:1stacks.ThisprocesstakesplaceinacidsoilenvironmentandAlforitisprovidedbyhydrolyticalterationofsilicates–primary,orthesameclaycomponents(Bamhisel&Bertsch1989).Presenceofthesecomponentsintheeluvialhorizons(insituinAlexandrovandredepositedinOberlaab)pointtoacidweatheringinbothinterglacialpaleosols.However,theal-ternative explanationofhigher contentof chloritic com-ponentintheupperhorizonsofacidforestsoilsonloessalsoexists.Jamagneetal.(1984)supposethattheseminer-alsarenotformedthroughthesynthesis,butratherbysim-plebreakdownandpartialdegradationofprimarychloritesfromsiltfractions.

Surfaceredoximorphic(stagnic)processesproducedfer-ruginous pedofeatures throughout the profile, but mostabundantandvariableintheeluvialandupperBthorizons.Theretheyarepresentedbynodulesaswellasbycoatingsandincrustations,indicativeofironmigration(Bronnik-ovaetal.2000).Besidesintra-horizontalshort-distancere-distributionwesupposecertaineluvial-illuvialtransportofironfromEtoEBandupperBthorizonsduetothisproc-ess.DithioniteextractableironisdepletedinEhorizonsandhasitsmaximumintheBt1;alsotheabundanceofthefer-ruginouspedofeaturesismaximalintheEBandBt1hori-zons.InterestinglymagneticsusceptibilityalsodemonstratesmaximainEB(Alexandrovquarry)(Rivasetal.2003)andBt1(Oberlaab)(Solleiroetal.2013,thisvolume)thatcouldalsoberelatedtotheincreaseofpedogenicironoxides.Itshouldbe taken into account that surface redoximorphicprocessescouldalsocontributetoacidweatheringandHIVneoformationthroughtheprocessofferrolysis(Brinkman1970).

Beingsimilarregardingthesetofthepedogeneticproc-esses the studiedpaleosolsdiffergreatly in their relativedevelopment. The Austrian paleosol demonstrates muchstrongerclayilluviationintheBthorizon,whereastheRus-sianprofilehasmuchstrongerevidencesofeluvialandsur-faceredoximorphicprocesses.Thistendencybecomesevenclearerbycomparisonwiththemodernsoils.TheEemiansoilinOberlaabhashigherclaycontentandmoreabundantclayilluvialpedofeaturesthantheoverlyingHoloceneLuvi-sol(Solleiroetal.2013,thisvolume).TheMikulinoAlbelu-visolinAlexandrovquarrycomparedtothelocalHolocenesoil,aHaplicChernozem,showscontrastingqualitativedif-ferencesinthesetofkeypedogeneticprocesses.TheCher-nozemischaracterizedbyhighaccumulationofdarkhumusanddevelopmentofcoprogenicgranularstructureresultinginthedevelopmentofMollictopsoilhorizon.Below,intheBkhorizonabundantneoformedcarbonatesareobserved.Morphologicalfeaturesofclaytranslocationareveryfew(ifany),claycontentisratheruniformthroughouttheprofileshowingnotendencytowardseluvial-illuvialdifferentiation(Gerasimovaetal.1996;Bronger2003).Thissetofpedog-enetispropertiestypicalforsteppepedogenesisunderUsticsoilmoistureregime(Bronger2003)providesundoubtedevidencethatonthelocalscaletheHoloceneclimatehasbeendrierthanthatofthelastinterglacial–inagreementwiththeabovementionedreconstructionforEasternEu-ropebyMorozova(Morozova1981;Morozovaetal.1998).ForcurrentresearchitisinterestingtocomparethestudiedMikulinoprofilewiththenearestanaloguehavingsimilarprofileorganization, toassess changes in theAlbeluvisolpedogenesisontheregionalscale.TheMikulinoAlbeluvisolinAlexandrovquarrycomparedtotheHoloceneAlbeluvi-soloftheMoscowregion(Targulianetal.1974b),doesnotshowstrongerclayaccumulation,whichiscontrarytothecasestudyinLowAustria.However,itdemonstratesma-joradvanceofeluvialandstagnicprocesses–bleachingandclaydepletionbesidesEandEBhorizonsaffectedthewholeBthorizon,“attacking”theareaofearlierclayilluviation.FreshilluvialpedofeaturespointingtoactiveclayilluviationappearonlyinthelowerBt2andBtChorizons.InprofilesofHoloceneAlbeluvisols(Kühnetal.2006)andGreyForestSoils(Miedemaetal.1999)this“aggression”ofeluviationagainstdegradingilluvialareasisalsoobservedbutusuallyisnotsodeep.ItisstronginEBthorizonanddecreasesintheupperpartofBthorizons,whereitisrepresentedmostlybydeepthinbleachedtongues(albeluvictonguing),whereastheareasbetweenthetonguesaremuchlessaffected(Spiri-donovaetal.1999;Saueretal.2009).Thus,inbothcaseslastinterglacialpaleosolspresenthighergradeofdevelop-mentthananalogousHoloceneprofilesintheregion,how-ever,theparticularmodeofthistendencyisdifferent.

These differences could be explained when linked totheclassicevolutionschemeforforestsoilformationun-dertemperatehumidclimate(Pédroetal.1978).FollowingthisschemeintensiveclayilluviationdevelopsafterinitialleachingphaseandresultsintheformationofArgichorizon.However,itissucceededbythesubsequent“degradation”stageoffurtheracidification,surfaceredoximorphicproc-essesand(possibly)ferrolysis.Atthisstageclayilluviationishamperedandpartofaccumulatedclayislostduetoacidweathering.WesupposethatEemianLuvisolinOberlaab

Horizon Grain size fractions, % Fed, %

sand silt clay


WP upper 5.4 68.5 26.1 0.69

WP lower 8.2 69.8 22.0 0.65

Btg1 10.1 66.7 23.2 0.98

Btg2 6.3 55.9 37.8 0.73

BCtg 4.6 60.9 34.5 0.61

BCg 4.3 64.4 31.3 0.37

C 5.7 65.4 28.9 0.50


A 1.4 81.8 16.8 0.49

E upper 1.4 88.7 9.9 0.22

E lower 1.2 86.5 12.3 0.32

EBt 1.1 79.3 19.6 0.43

Bt1 1.0 78.2 20.8 0.51

Bt2 1.2 70.3 28.5 0.45

Bt3 1.5 76.1 22.4 0.43

BC 1.2 80.0 18.8 0.37

WP – Würmian pedosediment

Tab. 2: Grain size distribution and dithionite extractable iron content.

Tab. 2: Korngrößenzusammensetzung und dithionitlöslicher Eisengehalt.


stilldevelopedwithinthestageofpredominantclayforma-tionandilluviation,whereasMikulinoAlbeluvisolinAlex-androvquarryalreadyreachedthestageof“degradation”.

Thisdifferenceintheevolutionarystatusismostprob-ablyrelatedtothecompositionofthepaleosolparentmate-rial.TheRissloessinAustriaisricherinweatherableminer-als(includingphyllosilicateslikebiotite),hasmoreclayeytexture,isenrichedinbasesandhaslowerSicontent.Thisincreasesthepotentialforneutralizingexcessiveacidityaswellasfortheneoformationofclayandironoxides.TheDnieperloessinmuchpoorer,stronglyenrichedinquartz,thusbufferingandclaygeneratingcapacitiesarelower.

Chronological and paleoecological background of the advanced Eemian/Mikulino paleosol developmentOnthelocalscale,especiallyintheborderregions,quali-tativedifferencesbetweenMikulino/EemianpaleosolandmodernsoilprofileareclearlyrelatedtoclimaticshiftasshownbythecaseofAlexandrovexposure.Thequestionarises,whatarethereasonswhylastinterglacialpaleosolsdemonstratemore advanceddevelopment thanHolocenesoilsbelonging,however,tothesametypeofpedogenesis(provenbysimilarityofhorizonation,mainmacro-andmi-cromorphologicalcharacteristics,claymineralassociationetc.)?Wesupposethatinmanycasesthedurationofpedo-genesisratherthan“stronginterglacialpaleoclimatesrela-tivetothepresent-dayclimate”(assupposedbyMahaneyetal.1993)couldaccountforthesedifferences.ComparisonwiththeEuropeanpaleobotanicalrecordswithhigh-reso-lutionchronologicalscaleprovidesinsightintothisprob-lem.DetailedcorrelationwiththedeepseaisotoperecordsandestablishingtheprecisepositionofBlakepaleomagneticeventallowedreliabledatingofthemainpaleobotanicphas-esofEemianestablishedearlierinthepollenspectrafromterrestrial (mostly lacustrine) sediments (Zagwijn 1996;Turner2002a).EarlierthelastinterglacialwasassociatedwiththeMarineIsotopeStage(MIS)5e(Shakleton1969).Recently,itwasshownthatthespreadofforestvegetationinEuropepostdatedtheonsetofMIS5ebutontheotherhand

extendedintothesubsequentstage5ddespitethebeginningofglobalcooling,increaseoficevolume,anddropofsealevel(Shakletonetal.2003;Sieretal.2011).Thisextensionconcernsinparticularthelast“post-temperate”paleobotani-calphaseofborealforests.Thus,althoughthedurationofthelastinterglacialsensustrictoissupposedbymanyauthorstobeabout11000yr(similartothatoftheHolocene)(Casp-persetal.2002;Turner2002b),thetotalsuccessionoftheEemianforestvegetationphasesintheWesternandCentralEuropecouldreach20,000yr-nearlytwicelongerthantheHolocene(Kuklaetal.2002).

Itshouldbestressedthatallphasesofhumidforesteco-systemsincludingthelastoneoftheborealforestsprovideconditions for clay illuviation and development of Argichorizonsonloess-likesediments.Thus,thescenariooflong-termclayilluviationduringthecompletesuccessionofdif-ferentforestphasesduringMIS5explainsmoreadvanceddevelopment of Eemian/Mikulino paleosols compared tothe Holocene analogues. Rather cold climatic conditionsduringthelaststagesofAlbeluvisolprofiledevelopmentinCentralRussiaare confirmedbymicromorphologicalob-servations.Typicalfeaturesofeluvial-illuvialprocessesarecombinedwithdeepfrosteffectsintheupperpartoftheprofile.Lenticularstructurewiththemicroscalegrainsizedifferentiationisrelatedtoicelensing(vanVliet-Lanoë2010), iron incrustations of the platy aggregates are alsocharacteristicforseasonallydeeplyfrozensoils(Fedorova&Yarilova1972).

Anevenmorecomplexscenarioforinteractionofilluvi-alandfrostprocessesisrequiredfortheEemianLuvisolinOberlaab.Here,theilluvialandfrostfeaturesnotonlyco-existbutshowcomplexinteraction.Frostfracturingpropa-gatesintotheBthorizondisruptingtheoldergenerationofthe clay illuvial pedofeatures and generating blocky-len-ticularstructure,whereastheyoungergenerationofclaycoatings covers these aggregates. The clay translocationprocessitselfwasheterogeneousasevidencedbyvariablecomposition of illuvial pedofeatures. Impure dusty andcoarse clay coatings (“mud cutans”) are attributed to the

Horizons Types of clay minerals

Smectite/ illite Illite / smectite

Chloritised 2:1 minerals

Illite Kaolinite


WP upper - xxx x xxx xx

WP lower - xxxx xx x x

Btg 1 - xxxx xx x x

BCtg xxxx xx - x x

BCg xxxxx x - xx x

C xxxxx x - xx x


E upper - xxx xx x xx

E lower - xx xx xx xxx

EBt - xx xx xx xx

Bt2 xxxx xx - x x

C xxxxx - - x x

Tab. 3: Clay mineral composition.

Tab. 3: Tonmineralogische Zusammensetzung.

WP – Würmian pedosedimentxxxxx – dominantxxxx – abundantxxx – frequentxx – fewx – traces- - not detected


fastpercolationof suspensions after snowmelt in freeze-thaw soils (van Vliet-Lanoë 2010). The laminated claycoatings(whichweobservedinthelowerpartoftheEemi-anLuvisolofOberlaab)wherepurelimpidandimpuresiltymicrolayersarejuxtaposed,couldbeinterpretedasalter-nationof“normal”illuviationduetoslowpercolationandfastdeposition fromsnowmelt suspensions (Kühnetal.2010).

ThissuggeststhatclayilluviationintheOberlaabpro-filewaspolygeneticanddiscontinuous,interruptedbythestagesofdeepfrostprocesses.SuchinterplayoffeaturesiswellknownforQuaternaryBthorizonsandcouldbeusedforpedostratigraphicinferences(summarizedbyvanVli-et-Lanoë2010)

Concerningpossiblechronologicalandpaleoecologicalimplicationsweshouldtakeintoaccountthatnopaleosols

orpedosedimentsclearlycorrespondtotheEarlyWürmianinterstadials.Thus,wecouldsupposethatthepedogenesisofthesewarmerstagescouldcontributetotheformationofthe“Eemian”profileinOberlaab.InseveralprofilesofEu-ropethesoilsoftheseinterstadialsarecharacterizedbydarkhumusaccumulationandcorrespondtosteppeenvironment(e.g.MosbacherHumuszoneninGermany,KrutitsasoilinRussia,etc.).Fromsuchtypeofpedogenesisonewouldnotexpect contribution to theclay illuviation.However, thistypeofsoilandlandscapeconditionsseemstobenotsoleduringtheEarlyWürmianinterstadials.ForestecosystemshavebeenalsoregisteredbyvariousEuropeanpaleoecologi-calproxies(Bibusetal.2002).Thewarmerclimateandrefor-estationcouldprovideconditionsforLuvisolpedogenesis,althoughinterruptedbycoldphasesoftheearlyglacial.Ear-lyWürmianBthorizonsclearlyseparatedfromtheEemian

Fig. 6: X-ray diffraction patterns of oriented air-dry specimens of clay frac-tions from selected paleosol horizons; a) Oberlaab profile, b) Alexandrov profile.

Abb. 6: Röntgenbeugungsdiagramme von orientierten luftgetrockneten Proben der Tonfraktion aus ausgewählten Horizonten der Paläoböden; a) Profil Oberlaab, b) Profil Alexandrov.


LuvisolandcorrelativetoMosbacherHumuszonenwerere-portedintheRhineArea(Leser1970).Asmentionedabove(see‘Introduction’)severalauthorsdescribedsuperimposingoftheEarlyWürmianclayilluviation(associatedwithGreyForestSoilformation)overthepre-existingEemianLuvisolproducingapedocomplex.

WesupposethatEarlyWürmianclayilluviationcoulddevelopinthe“Eemian”ArgichorizoninterruptedbyfrostprocessesimposedbythecoldstadialsinOberlaab.Thus,itsmorphologicalandanalytical(claycontent,geochemicaldifferentiation)characteristicscouldbeanintegraloflongerLuvisolpedogenesisincludingEemianInterglacialsensulato(MIS5eandpartofMIS5d)andEarlyWürmianinterstadials(correlativetoMIS5candMIS5a).SuchcumulativeeffectcouldbepresentinanumberoftheEemianLuvisolpro-fileswhereEarlyglacialsedimentationwasnotsufficienttoseparateinterglacialandinterstadialsoilbodies.InthiswaywereturntotheearlierideasofBoardman(1985)whostat-ed:“Geologicalandpalynologicalevidencefromterrestrial,midlatitudesitessuggeststhattemperateconditionscondu-civetosoilformationexistedforperiodsgreatlyinexcessof10,000yrduringthemiddleandlatePleistocene.Avail-abledataonsoilsformedduringthisintervalfromWesternEuropeandmidwesternUnitedStatesarebestexplainedbyrelativelylonginterglaciationsorthedevelopmentofcom-positesoilsoveranumberoftemperateperiods”.

Acknowledgements

Wewouldliketothankallcolleagues–scientistsandstu-dentsfromAustria,Germany,MexicoandRussiawhotookpartinthefieldandlaboratoryresearchoftheICSU2003project “Polygenetic models for Pleistocene paleosols”and generated a productive and friendly atmosphere oftheproject sessions.Wearegrateful to the InternationalCouncil of Science (ICSU) whose funding made possiblethis wonderful experience of intensive interdisciplinaryandinternationalcollaboration.SpecialthanksareforProf.WinfriedBlumwhoencouragedusat the initial stageofthe ICSUProjectdevelopmentandprovidedvaluablead-vicesandsupport.

We would also like to express our gratitude to Direc-ciónGeneraldeAsuntosdePersonalAcadémico,UNAM(DGAPAUNAM)forfundingthesabbaticalstayofS.Se-dovintheUniversityofWürzburg,allowingtofinalizethisresearchandtopreparetheresultsforpublication.

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Abstract1 Introduction2 Materials and methods3 Results4 DiscussionAcknowledgementsReferences

sergey sedov, svetlana sycheva, victor targulian, teresa ... › articles › 62 › 44 › 2013 ›...

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