sign in sign up
<<
Home , Aar (Lahn), Flensburg, Michelbach (Usa), Nister (river), Palatinate Forest, Truncated upland

Vol. 144, No. 1 · Research article

Quantification and dating of floodplain sedimentation in a DIE ERDE Journal of the medium-sized catchment of the Geographical Society of German uplands: a case study from the Aar in the southern ,

Christian Stolz1, Jörg Grunert2, Alexander Fülling3

1 Interdisziplinäres Institut für Umwelt-, Sozial- und Humanwissenschaften, Abteilung Geographie, Universität Flensburg, Auf dem Campus 1, 24943 Flensburg, Germany, [email protected] 2 Geographisches Institut, Johannes Gutenberg-Universität Mainz, 55099 Mainz, Germany, [email protected] 3 Geographisches Institut, Humboldt-Universität zu Berlin, Unter den Linden 6, 10099 Berlin, Germany, alexander. [email protected]

Manuscript submitted: 23 May 2011 / Accepted for publication: 12 April 2012 / Published online: 2 September 2013

Abstract The distribution, thickness and composition of the floodplain sediments in the valleys of the Aar and its tributaries ( Mountains) were investigated by way of extensive fieldwork at 25 locations. In the entire catchment area, 48.8 million tons of loamy floodplain fines could be assessed. Most of these were deposited since late medieval times due to extensive historical land use and clearing, especially in the region along the middle course of the Aar. In its lower course, the enhanced sedimentation of loamy floodplain sediments started during the .

Zusammenfassung Die Verteilung, Mächtigkeit und Zusammensetzung der Auelehme in den Tälern der Aar und ihrer Neben- flüsse wurden im Rahmen ausgedehnter Geländearbeiten an 25 Standorten untersucht. Im gesamten Ein- zugsgebiet der Aar konnten insgesamt 48,8 Mill. t Auelehm erfasst werden. Der Großteil davon wurde seit dem Spätmittelalter als Folge der historischen Landnutzung und Entwaldung, insbesondere im Berg- baugebiet am Mittellauf der Aar, sedimentiert. Im Unterlauf der Aar begann die verstärkte Sedimentation von Auelehm bereits in der Bronzezeit.

Keywords Alluvial sediments; dating and budgeting; Taunus Mountains; Aar River; mining region

Stolz, Christian, Jörg Grunert and Alexander Fülling of the German uplands: a case study from the Aar Valley in the southern Rhenish Massif, Germany – DIE ERDE 144 (1): 30-50 : Quantification and dating of floodplain sedimentation in a medium-sized catchment

DOI: 10.12854/erde-144-3

30 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

1. Introduction (Oberpfalz, eastern ), Raab et al. (2010) de- - 1.1 The formation and characteristics of floodplain mer mining, deforestation and smelting when sediments theytected found historical respective overbank contamination fines as the resultwith ofheavy for metals. The situation in the Vils area is similar to that in the Aar catchment. Furthermore, recent stud- ies and reviews in various Central European regions The deposition of loamy overbank fines results from have rendered similar results (Stolz et al. 2012, Stolz aphases catchment with (cf. accelerated Hoffmann fluvial et al. activity,2010). Along in reaction larger 2011a, Stolz 2011b, Stolz and Grunert 2010, Hoffmann to either climatic or land-use related influences to et al. 2010, 2008, 2007, De Moor and Verstraeten 2008, Houben et al. 2006, Klimek et al. 2006, Coulthard et al. clearlyrivers, evidenced climatically (Schirmer caused et Early al. 2005). and Mid-HoloceneRepeated dis- 2002, Heusch et al. 1996, Pörtge and Molde 1989). As placementfloodplain of deposition river branches and erosionwith lateral phases deposition could beof not every single event which triggered soil coarse levee sediments and the horizontal deposition colluvia deposits on the slopes may be used instead (cf.can Borkbe evidenced and Kranz by 2008).floodplain Niller profiles, (2001) in evidenced many cases in of silty overbank fines caused the formation of several the Kleine Laber catchment (eastern Bavaria) that the Holocene river terraces which can be identifiedMäckel in1969, the - middlefield as Lahnsmall River).steps. However,Within smaller these maycatchments be covered the horizontaland leveled sedimentationby younger overbank predominates, fines ( but - comparedHolocene colluvium the sequence could of beseveral much serially older than connected the al sedimentluvial deposits stores within with a the system same of fluvial cascades. catchment. He as well. In many catchments, 2-3 superimposed gen- and gravel-filled palaeochannels can be evidencedBrosche 1984; Neumeister 1964). 1.3 Open questions and approaches erations of overbank fines were proven (e.g.

1.2 Triggering of soil erosion by deforestation and Aar and its tributaries in detail. The focus is on iron industries theThis genesis study investigates and the age ofthe these loamy sediments overbank of fines potential of the- ly anthropogenic origin, which leads to the following In the catchment of the Aar River (Taunus Mountains) questions: When did the sedimentation start, and dur- excessive soil erosion as a result of various kinds of ing which periods was it most effective? What were the land use was a major problem of the past. This was main triggering factors, anthropogenic or natural, and predominantly caused by the strong deforestation how effective was the impact of the local iron industry? for iron smelting in the local ironworks of Michelbach sections, and how strong was the preceded soil erosion small, decentralised iron-smelting works which exist- How much sediment was accumulated in different river ed(since before. 1656 Particularly AD; Michelbacher on the Hütte)slopes andin the in numerouswide mid- sediments can be distinguished and, moreover, dle reaches of the Aar, gullies up to 10 m deep, young arein the they catchment? visible as lowFurthermore, terraces? which types of flood- alluvial fans and colluvial layers are widespread (Stolz 2008, Stolz and Grunert 2006). Regarding these facts, Reliable written sources about phases of sedimenta- the considerable thickness of up to 5.5 m of the loamy tion in the Aar area do not exist. Therefore, we used Auelehm primarily radiocarbon datings of plant residues em- isand not gravel-free surprising, overbank however, fines it is ( distinctly, flood above-av loam)- completed by Optically Stimulated Luminescence eragein the whenfloodplains compared of the with Aar otherRiver riverand its systems. tributaries The (OSL)bedded datings. in the Morefines. reliable Furthermore, datings these could results be obtained were in combination with historical reports such as the of the widespread loess-rich periglacial cover-beds in thelarge catchment amount of (cf. fines Semmel can be1968). explained by the erosion it was possible to involve pond sediments and histori- specific land use of an area at a given time. InStolz one caseand In eastern Belgium, the early modern iron industry Grunert describedcal slag deposits and discussed in the Aar regarding floodplain their (cf. formation iron slag (Gautier et al. 2009). In the Vils catchment and human 2008). impact. Typical Based profiles on this of the knowledge, floodplains it was are triggered the formation of overbank fines containing DIE ERDE · Vol. 144 · 1/2013 31 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Tab. 1: The beginning of anthropogenically affected floodplain deposition in various parts of Germany

Catch- Earliest No. Region River Dating methods Authors ment deposition

Basin of Leipzig Radiocarbon, 1 Weiße Elster Saale 3000 BC Tinnap et al. 2008 (Saxony) archeological

Leine Hills Older 2 Leine Weser Pollen Pretsch 1994 (Lower Saxony) Subboreal

Weser Hills Younger 3 Upper Weser Weser Pollen, radiocarbon Thomas 1993 (Lower Saxony) Subboreal

Black Forest Mts. Dreisam, Basin Upper Mäckel and 4 1500 BC Radiocarbon (Baden-Württemberg) of Zarten Rhein Friedmann 1999

Palatinate Forest 5 1300 BC Radiocarbon Stolz 2011b (Rhineland-)

Lower Bavaria 6 Vils Donau 1200 BC Radiocarbon Raab et al. 2005 (Bavaria)

Lower Bavaria 7 Kleine Laaber Donau 500 BC Radiocarbon Niller 2001 (Bavaria)

Wetterau Basin Lang and Nolte 8 Main 250 BC IRSL () 1999

Franconian Switzerland 9 Aufsess Main 400 BC OSL Fuchs et al. 2010 (Bavaria)

Marburg/Gießen area Younger Iron Radiocarbon, 10 Rhein Urz 2003 (Hesse) Age archaeological

Alpine Foothills 11 Lech Donau 100-400 AD Archaeological Dietz 1968 (Bavaria)

Lower Mts. 12 Gelbach Lahn 400 AD Radiocarbon Stolz 2011a (Rhineland-Palatinate)

Solling Mts. 700 AD (at 13 Ilme Weser Pollen, radiocarbon Rother 1989 (Lower Saxony) the latest)

Volcanic Mts. 700 AD (at Radiocarbon, 14 Lieser Mosel Stolz et al. 2012 (Rhineland-Palatinate) the latest) archeological, OSL

Wetterau Basin 15 Wetter Main 850 AD Radiocarbon Houben 2002 (Hesse)

High Westerwald Mts. Radiocarbon, 16 Große 900 AD Stolz 2011a (Rhineland-Palatinate) archeological

possible to calculate the total amount of overbank with the knowledge about two streams in the Wester- wald Mountains and one in the Palatinate Forest. stated in tons and in cubic metres (see Sections 5 and 6).fines Moreover, stored inthe the results Aar catchment.from the Aar The will results be quan are- 2. State of research catchment, knowing that we cannot make any clear statementtified concerning about the the sediment eroded soiloutput material from the from catch the- Natermann (1941) and Mensching ment in general. Finally the example will be compared (1951) were the first 32 to identify loamy overbankDIE fines ERDE as · anthropogenicVol. 144 · 1/2013­ a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

in the early settled Wetterau depression, 60 km east of the Aar valley. They determined the maximum sedimentation rates for the Early since 750 AD. In the early settled regions of Germany, hu- man impact on the landscape occurred at least in the Early Neolithic (ca. 7500 BP; Dotterweich et al. 2008). In the Lowlands of Leipzig (Central Germany) Tinapp et al. (2008) evidenced that the start of anthropogeni-

3000 BC. The wide differences concerning the start of cally introduced floodplain deposition began around different German regions are presented in Table 1. ­anthropogenically affected floodplain deposition in After the disintegration of the Roman Empire at the end of the 3rd century AD, many parts of Germany became reforested (Bork et al. 1998: 221). This can also be applied to the Taunus Mountains since the Roman runs through the upper part of the Aar Fig. 1 Location of the Aar catchment in Rhineland-Palatinate and catchment. For some time afterwards, pollen studies Hesse (cartography: T. Bartsch, Mainz ) by Hildebrandt et al. (2001) in the Lower Westerwald Mts., located 25 km north of the Aar catchment, have Hövermann (1953) added - - dle Ages. This was followed by a reforestation phase allysequence influenced of anthropogenic sediments. land use. Hempel (1959) shownduring thea low Late level Middle of woodland Ages (spätmittelalterliche during the High WüsMid- that overbank fines were not only deposited in con tungsperiode, cf. Born 1989). Schmenkel (2001) discov- Germany into four different types: ered the largest proportion of non-tree pollen for the divided the flood-plain sediments of rivers in Central 1. late glacial loams and loesses, partly interlocked with Weichselian gravel above bedrock; High Middle Ages, in the Valley, east of the Aar. 3. Regional setting 2. late glacial loams or loesses which are displaced by The Aar River drains the central part of the Taunus Mountains, representing the south-eastern part of the fluvial activity; - Rhenish Massif (Taunus Mountains). This area drains pogenically caused soil erosion on the slopes; and into the rivers Lahn and and is bordered in the 3. older overbank fines which are the product of anthro east by the Wetterau depression, north-east of Frankfurt - (Fig. 1). The Aar passes through the Taunus Mountains thropogenic soil erosion on the slopes. from its southern rim (quartzite range) near the city of 4. younger overbank fines resulting from young an Wiesbaden into the Lahn River in the north near Limburg Generally, it is not easy to differentiate between sedi- an der Lahn. The catchment comprises a total of 312 km². ments triggered by anthropogenic soil erosion and Variscan metamorphics, mainly clayey and Taunus quartzite are forming the bedrock in the upper reaches. - The deeply incised middle reaches of the valley have a cenenatural (cf. floodplainSeidenschwann’s sediments. investigations In fact, even(1989) gravelly in the difference in altitude of nearly 180 m as compared to the sedimentsKahl catchment, could havenorthern been depositedSpessart Mountains, during the Holowith surrounding peneplains, interpreted as palaeosurfaces from the Mesozoic and Tertiary (cf. Andres 1967).

Mid-Holocene gravel deposition). Nearly all valley slopes are covered by periglacial slope sedimentation differs substantially in various catch- deposits ( and Felix-Henningsen 2006, ­Kleber mentsThe beginning in the German of the uplands anthropogenically (Dreibrodt et influenced al. 2010). 1997, Semmel 1968) consisting of a debris-rich basal Lang and Nolte (1999) asserted that the start of the layer, one or several more or less loessic intermediate deposition began in the Late Iron Age/Roman Period layers, and a loess- and debris-containing upper layer.

DIE ERDE · Vol. 144 · 1/2013 33 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

On many exposed slopes within the Aar catchment and The moderate climate of this region is characterised at the rim of the quartzite range of the Taunus Moun- by cool and humid winters and warm summers with tains, the middle layer may be missing. In the middle average temperatures of -1.9 to 1.0°C (January) and and lower reaches of the Aar skeleton-free loesses were found at some locations. The periglacial cover- ner and Wiesbaden, period 1961-1990, Mühr - 2007).14.3 to The 17.4°C mean (July; annual meteorological precipitation ranges offices between of Klei­ sulting from anthropogenic soil erosion, in downward- 800 and 900 mm and a thin layer of snow is quite com- slopingbeds are positions regularly as covered well as onby terracesHolocene ( Stolzcolluvium 2011c). re mon in January and February.

Tab. 2: Quantification of soil erosion using data of floodplain sedimentation in the Aar catchment

34 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Tab. 3: Datings from the Aar floodplain

4. Materials and methods largely followed the standards of the international 4.1. General methods Worldpoints wereReference tachymetrically Base for Soil surveyed. Resources This 2006fieldwork (In-

More than 150 drillings were cored, at 14 locations ­German Bodenkundliche Kartieranleitung, 5th edition in the Aar valley and its tributaries, to a depth of as (Ad-hocternational AG BodenUnion 2005)of Soil wasSciences used 2006).for the Thedescription official much as 8 m, and more than 30 pits were dug along of genetic soil features. Soil colours are described af- ter Munsell Colour Company (1990). severalDIE ERDE drilling · Vol. 144 series · 1/2013 in the floodplain. All sampling 35 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Further data of drillings from 11 other locations, which By this procedure and the addition of the subtotals, have been cored since the 1930s and catalogued by the be calculated for the whole catchment. the amount of recent available overbank fines could Geologie),drilling archives were incorporated. of the Hessian The Office interpretation of Environment of the and Geology (Hessisches Landesamt für Umwelt und 4.3 Optically stimulated luminescence (OSL) ­dating of geological procedure (cf. Seidel and Mäckel 2007). data was partly difficult due to the different techniques Using OSL, it is possible to date the most recent day- Afterwards, the samples were analysed for their gran- light exposure of mineral grains which occurred nor- ulometry (Köhn mally during sediment transport prior to deposition. (CaCl2), carbonate content (Blume 2000) and in some Thus, OSL is an appropriate method to estimate the ), organic matter (loss on ignition), pH geo ­morphological processes by dating their related - separatedcases also forfrom their the heavy-mineral sediments by contentan archaeo-botan of the fine-- plete resetting of the luminescence signal before burial sandical elutriation fraction (0.063-0.2 procedure µm). (Jacomet Charcoal and samples Kreuz 1999). were sediments, e.g. loamy overbank fines. However, incom- Schwein­ vial environments. To circumvent this problem, differ- gruber 1990) and some samples as well as other or- entcan approacheslead to age haveoverestimation been proposed, often such observed as the inuse flu of ganicThey wereresidues identified could beunder radiocarbon-dated the microscope (AMS( dat- single grains or small aliquots containing only a limited ing, calibrated by the data sets of Reimer et al. and number of grains (e.g. Wallinga 2002, Jain et al. 2004). Intcal04; cf. Stuiver et al. 1998). Five sediment sam- ples were dated in the laboratory of the Department In this study, OSL dating was applied to small multi- optically stimulated luminescence (OSL) (Tab. 3). After separating the required grain size fraction by of Geography at Humboldt University in Berlin using wetple-grain sieving, aliquots carbonates of sand-sized and organic matter (90-200 were µ m).re- - 4.2 Calculations for the quantification of ­floodplain sediments wasmoved then using extracted hydrochloric by density acid (10 separationand 30%) and using hy lithiumdrogen peroxidepolytungstate (10 and heavy 30 %), liquid respectively. (LST, 2.75 Quartz and 2.62 g/cm³). The following treatment with hydro- sectionsDue to the in altitudeorder to andquantify width the of amountthe floodplains, of overbank the contamination and removed the alpha ir- Aar and all its tributaries were classified in 16Tab. river 2). radiatedfluoric acid outer (40 %, layer 60 of min) the eliminatedquartz grains. any potentialAfter re- sheetsfines eroded 1:25,000, from the the totalslopes length in the ofcatchment each valley ( sec- were prepared containing approx. 200 grains each. Basedtion was on recorded. field results Furthermore, and the German the average topographic widths Thisnewed number sieving of (90 grains µm) issmall assumed multiple-grain to be appropriate aliquots Fuchs and Wagner and on maps (up to 15 measurements per section). 2003). Positively skewed multimodal palaeodose Theof uniform third necessary floodplains variable were is determined the average in thickness the field to detect insufficient bleaching ( of each section, which was calculated by the collected were in fact heterogeneously bleached prior to depo- data. Finally, we calculated the total volume of each sition.distributions In order revealed to select that the thebest floodplain bleached grainsediments pop- river section by means of the following formula: ulation, the minimum age model (MAM) by Galbraith

Volume of overbank fines in river section x ages have to be considered as maximum ages. = length × average width × average thickness et al. (1999) was applied. However, the resulting OSL All OSL measurements were performed on a Risø The following values were assumed for some small TL-DA 15 reader using the standard single-aliquot tributaries, which were not studied in the field: an regenerative dose (SAR) protocol (Murray and Wintle­ average floodplain width of 50 m and 100 cm as an 2000). The prepared quartz aliquots (sets of 24 to average thickness of overbank fines (Tab. 2). The 48 aliquots per sample) were stimulated with blue value of 100 cm is based on several field obser- LED light (e = 470 ± 30 nm) at 125°C for 40 s, and the vations in the Aar catchment. Their lengths were measured on topographic maps. - resulting OSL signals were recorded through a Hoya 36 U 340 filter (e = 330 ± 40 nm).DIE TheERDE preheat · Vol. 144 tempera · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 2 Typical profiles of the Aar floodplain at 25 investigated locations which show the distribution and characteristics of the floodplain ­deposits. Each profile has been selected from 2 to 30 drillings and excavations (data of sites No. 7, 8, 9, 11, 16, 17, 18, 20, 22, 23, 25 by Hessisches Landesamt für Umwelt und Geologie, drilling archive; cartography: S. Böhnke).

DIE ERDE · Vol. 144 · 1/2013 37 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands: ture was set to 200°C (10 s), the test dose cut-heat The former assumption that the thickness of the grey- performing preheats and dose recovery tests on the Aar River near Freiendiez could reach 8 m, which temperature to 160°C. These settings were verified wasbrown reported sandy overbankby the former fines German in the lowerInstitute reaches of Soil of Researches (Reichsstelle für Bodenforschung) in 1937 Thesamples sediment HUB-0136 dose andrates HUB-0137. were estimated by meas- (cf. Stolz and Grunert 2008), proved to be wrong. In the uring the contents of uranium, thorium and potas- summer of 2010, this was disproven by several 6 m deep sium, then applying neutron activation analysis drillings at the same place. Four m of sandy overbank (Becquerel Laboratories, Mississauga, Canada). The cosmic-ray dose rates were estimated from Very clayey saprolithic slates were found at a geographic position, elevation and burial depths depthfines are of underlain6 m. It is bypossible a gravel that layer in more1937 thanthe geologists 2 m thick. (Prescott and Hutton 1988, 1994). - wise, they could have interpreted the grey saprolithe as drilled into the loamy filling of a former stream. Other 5. Results overbank fines below the local level. - - ies ranges between 4 m at the Aubach and only 0.8 m ied at 25 locations between the upper reaches and the atThe the thickness smaller ones.of floodplain sediments of the tributar lowerThe floodplain reaches ofsediments the main of valley the Aar and River locally were on stud the - guished by their position in the landscape, their valley 5.2 A typical sequence of floodplain sediments floodplains of some tributaries. All sites can be distin- eas (Fig. 2 According to the explanations to the German geologi- toshapes the bridge and their near widths the village of the floodplainsof Seitzenhahn in six (3 subar loca- cal map 1:25,000 (No. 5714 and 5614), Koch and ­Kayser tions), and): the the middle upper reaches withfrom aTaunusstein-Hahn deep and narrow - v-shaped valley from Adolfseck to Michelbach; further- more, the middle reaches with a more expansive valley (1881,They characterised 1886) were the the firstaccumulations to assume intoan Early 3 types: Holo from the estate of Michelbach to Zollhaus, and the low- cene age for the overbank fines in the Aar catchment. point, is broad at the beginning (up to 500 m) and be- Niedern­eisen (Fig. 2 comeser reaches narrower from therefurther to downDiez. Thethe valleyvalley nearfloor the at thisvil- 1. Overbank fines, downwards of the village of ) aboveRiethboden the recent) closeflood to-level; the of the Middle and Upper Devonian. Three sites are lo- catedlage of in Holzheim, the longest due tributary, to more resistantthe Aubach, metamorphites whereas the 2. Humic overbank fines ( other, smaller tributaries contain seven sites. 3. Sriverandy in and the gravellyrecent flood alluvial area; sediments in the fre- Alluvionen der Tal­ ebenen). 5.1 The distribution of loamy floodplain ­sediments quently flooded locations ( in the Aar catchment During the recent investigations, in some places, a second, marginally higher floodplain level (50- Principally, the content of skeleton in the overbank 100 cm) could be monitored, which has not got - overrun by recent flood events (cf. the results of ally, the loams on the top are completely free of gravel. Heusch et al. (1996) from the lower Sieg River). fines tends to increase top-down in the profile. Usu These different floodplain levels are difficult to The thickness of the loams varies in the longitudinal recognise because they tend to ­occur sporadically. The top is formed by overbank fines. skeleton-free loams almost up to 2 m thick. In the narrowprofile ofpart the of valley. the middle In the reaches upper reachesthe thickness there aredi- Gravelly and sandy deposits as described by Koch and minishes to 1 m, whereas in the wide part of the lower Kayser (1886) could only be detected near to the rim middle reaches, where the valley enlarges, the regu- of natural, unregulated sections of the Aar River. Such lar thickness rises to 4 m and, locally, up to 5 m. In formations consisting of gravel and a thin cover of the lower reaches, the loams are on average 3 m thick.

38 loamy sediments on top can DIEbe identifiedERDE · Vol. as 144 levees. · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 3 A typical profile from the floodplain of the Aar River near the village of Rückershausen (50°26’ N, 8°06’ E; design: T. Bartsch, Mainz ­University)

On the basis of selected examples of the investigated rarely comprise humus or peaty material, but locations, we have reconstructed a typical top-down rather very clayey sediments at the base. In other vega/gley Fig. 2): profile for the floodplains of the Aar River (soil types sectors, thin layers of sand or fine gravel occur, , c.f. the profiles presented in - clayeywhich signifyin downward former direction. flood events. This At could some be places, an in- dicationit was noted of calmer that the conditions overbank of fines sedimentation become more on 1. blessrown-grey gravel content; humic sometimes overbank fines,with initial recently soil disfor- mationplaced during(aM horizon; flood cf.events, Ad-hoc skeleton-free AG Boden 2005); or with 4. Ra educed,still wooded very floodplain.wet and frequently sandy overbank 2. a horizon with rust-coloured and black oxidation marks in skeleton-free overbank fines, which to-no charcoal fragments (aGr horizon). is underneath the groundwater level for a few fines with a low-to-half gravel content and little- weeks per year. Along former roots or wormholes (macropores), the loam is grey due to reduc- exceptionally also up to 20 cm), partly loamy or tion (aGo horizon); 5. Winterspersedell-rounded by fine loamy gravel layers, (diameter underlain up by to coarse 8 cm, gravel (diameter up to 20 cm and more). 3. a grey reduced, skeleton-free, silty loam, perma- nently lying below the groundwater level (aGr ho- 6. Bedrock (unweathered or sparolithic). This de- rizon). It often comprises charcoal fragments and - rarer anthropogenic relics, like shards or hand- of the Aar and the Aubach and less so for crafted pieces of wood. Frequently, there are sand- scription is mainly representative of the flood

the smaller tributaries. However, at some sites DIEor ERDE gravel-filled · Vol. 144 · 1/2013 channels inside the loam, which modified sequences occur. 39 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 4 Cross-section of the Aar floodplain near the Felsentor mill (Fig. 2, No. 13)

To illustrate, we present the analysis of a typical 6 m 5.3.1 The floodplain near the Felsentor mill (narrow middle reaches) near the village of Rückershausen (Fig. 2, No. 4; analysis indeep Fig. drilling-profile 3 in the floodplain of the Aar River,- ly free of skeleton, down to a depth of up to 5 m. Until Aar near the Felsentor mill (50° 10’ 38’’ N, 8° 4’ 17’’ E; a depth). of The 0.4 clayey-silty m, the strong overbank clayey fines silt is are grey-brown complete Fig.The 2example, No. 13, shows Fig. 4 the), which relative was small investigated floodplain by of sev the- (10YR 4/4; soil colour after Munsell Colour Company south-east, a former undercut slope is visible. The oxides. Further down, the sediment becomes oxidised transecteral drillings. also provides Due to artificial evidence river that regulationthe Aar normally in the (10YR1990) due6/4) to as more seen thanby rust 2% stains of organic and, underneath,matter and iron ho- mogeneously grey (2.5 YR 5/1) due to reduction. Be- stream. Another former stream is recognisable in the tween 2 and 3 m deep, the clay content rises remarkably runs further east in a recent swampy and loam-filled date these forms since datable samples do not exist. This correlates with calm sedimentation conditions. At middle of the floodplain. However, it is not possible to 4.45to more m, thethan skeleton 30% indicating content arises change again. of sedimentation. This indicates - corporates some gravel as a result of more dynamic Due to the lesser widths of the floodplain, the loam in- purea change gravel of sedimentationlayer underneath. conditions. The content The fineof organic gravel dominant in the old streams. The thickness of the could have been displaced during flooding from the- loamsflow (jet ranges effect). from Stillwater 1.2 to 2.4 conditions m in the creeks.were only Near pre to roscopic remains of wood, charcoal fragments or other the river, probably regulated in Early Modern times, matter fluctuates throughout the profile. Partly mac distinguish them from roots. The solid basal layer of of some decimetres in height. largerpieces gravelsof plants was were not found. possible In tothe penetrate field it is bydifficult drilling. to the young overbank fines form a typical embankment

5.3.2 The floodplain in the Auwiesen near Hausen 5.3 Exemplary cross-profiles in the flood plain über Aar (wide middle reaches)

Fig. 5 valley are demonstrated (Fig. 4-6). shows a section near the river course (50° 15’ 13’’ N, Three cross-profiles from different sections of the The floodplain in this section is around 140 m wide. 40 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 5 Cross-section of the Aar floodplain near the village of Hausen über Aar (Fig. 2, No. 6)

8° 3’ 28’’ E, Fig. 2, No. 6). The mostly silty and – in the the dating of the nearby Untergrund meadows (Fig. 2; ­lower layers – sandy loams are 4.3 to 5.6 m thick. The No. 5), this result was not included in the following whole profile is poor in skeleton. Only a few channels, ­spatio-temporal quantification of floodplain sediments. filled with sand, fine gravel and sandy layers appear in 5.3.3 The floodplain near (lower reaches) wasthe profile. detected. At Macroremainsa distance of 25 of m plants away (but from not the the river, humid an acids;old channel cf. Niller with et al.a sandy 2001) filling from andthis alayer humic were layer dated above by The cross-section downriver from Oberneisen 14C to the age cal. 1520-1450 BC (Beta-287555; Bronze Photo 1 and Fig. 6) re­ presents about half of the floodplain east of the gravels (Fig. 5 (50° 10’ 35’’ N,river (180 m). 8° 4’ 14’’ E;In general, Reichelt (1953) found Age). The eastern part shows clayey overbank fines above that there is no relationship between sediment ). This indicates laminar flowing probably thickness and valley length. Händel (1969), howev- Theon a loamystill forested sediment floodplain. itself, at a depth of 94 cm, was dated er, could demonstrate that along the Weiße Elster (Saxony) overbank fines are very thick on large floodplains of meandering rivers. redeposition,by OSL to 80-460 which AD. was However, proven the by OSLa high measurement paleodose scatter.revealed Thus, insufficient the result bleaching has to during be interpreted the last sediment as the In the transect presented here, it is obvious that the maximum age. After comparing this case with that of modern regulated river is now running closer to the

DIE ERDE · Vol. 144 · 1/2013 41 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 6 Cross-section of the Aar floodplain near the village of Oberneisen (Fig. 2, No. 2) north-western slope than before. Four OSL samples 5.4 Quantification of floodplain sediments in the were taken from locations along the cross-section: two Aar catchment from the loams in the western part and one sample from a thin sand layer of the gravels underneath (Fig. 6). These datings yielded the stratigraphic ages of 1600- the results of the investigated locations were trans- Toferred quantify onto thethe nearly concerning skeleton-free river sections overbank ( Tab.2 fines,; methods described in Section 3.2). 1680 AD (90 cm; HUB-0135), 1520-1600 AD (115 cm;- HUB-0136)ern part of the and section 1410-1530 one OSL AD sample (140 cm,was HUB-0137)taken from A total of 32.5 million m³ or 48.8 million tons of over- from a sand layer embedded into fine gravel. In the east of 1.5, Hoffmann et al. 2007). The calculated area of the sandy filling of a former channel below the overbank bank fines was calculated (using a conversion factor fines. It was dated at the maximum age of 600-880 AD erosion area of 296.2 km². This results in an average Furthermore,(210 cm; HUB-0138) in the because channel-filling of insufficient lots bleaching. macro- erosionfloodplains amount was of16.43 1647 km² t/ha as or opposed 109.8 mm. to a The theoretical highest scopic charcoal fragments were found (1592 mg/L). amounts were accumulated in the wide middle reach- One of these was dated by 14C age to cal. 1220-1270 es and in the upper part of the lower reaches between the villages of Michelbach and Zollhaus (Tab. 2; Fig. 2). of the determination of the species in the charcoal AD (Beta-287556; High MiddleQuercus Ages). Thespec. results Fagus 5.5 Dating and spatiotemporal quantification of sylvaticaspectrum of are the 42%determinable (weight) fragments. Fagus, 33% syl- overbank fines in the Aar catchment vaticahalf-ring-porous did not reappear deciduous in woodsthe region and 25%before the Sub-atlantic period and is now the main component For the neighbouring catchment of the Wörsbach, of the potential natural vegetation. This proves 20 km east of the Aar Valley, Anderle (1991) examined ca. 4 ka BP (cf. Pott 1995). The dated small channel hasthat shown the deposits a reactivating are of Young phase Holocene of the former age, sinceriver fragmenta site in the from town the ofsilt Idstein was dated with to 80 cal. cm 1165-1285 of fluvial siltAD course, since the backfilling 2 m underneath the sediment above 105 cm of clayey-silty fine sand. A bone small channel is older (Fig. 6). was dated to cal. 575-777 AD (). By a (High Middle Ages). A piece of wood from the fine sand 42 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Photo 1 Aar floodplain near Obern­­­­­­­­­­eisen, view ­to­wards the south (Photo: Christian Stolz) corresponding pollen analysis the pollen volume of her- charcoal fragment at a depth of 174 cm in the skeleton- baceous plants amounted to 400 % of the tree pollen. Duefree overbankto these different fines to cal. dating 1033 - 1145 methods, AD it (Erl-6435). is possible ­narrow middle reaches of the Aar (Fig. 2, No. 12) In a construction pit near Burg Hohenstein in the ­spatially. Basically, even gravelly sediments could have Tab. 3; Stolz 2008). to quantify the floodplain sediments temporally and- ­geologists from the Hessian Geological Survey dated a eval charcoal fragment from Oberneisen originates Intree the log Schmidtwiesen to 970-1025 AD meadows, (Hv-19789; south of Michelbach, frombeen theaccumulated upper part during of a gravel the Holocene. layer below A Late the loamyMedi deposits. Nevertheless, due to this uncertainty in non- which had been dug in the older part of the overbank we dated charcoal fragments from a slag-filled pit dated profiles, we only used the loamy overbank fines Stolzfines and covered Grunert by younger floodplain sediments. The for quantification. In the river section from Wehen to charcoal was dated to cal. 1427 - 1471 AD (Erl. 8915; betweenthe Felsentor 1320 mill,and 45 %ca. 1850. of the In overbankthe section fines from were the 2008). Below the slag-filled pit, at the accumulated between 1000 and 1320 AD and 55 % Frombase of 1333 the overbank to 1820 fines,AD, an gravel artificial could bepond detected. existed near the village of Adolfseck (Fig. 2, No. 14). Its ForFelsentor the section to Michelbach from Michelbach the proportion to the Aar is 30 % estuary to 70 %. near clayey sediments are covered by 65 cm of younger Diez (Lahn River), we had to produce calculations with another time scale, which gave the following results: total amount of overbank fines in a comparable overbank­profile (Stolz fines. and These Grunert correlate 2008). with 55% of the 46 % of the skeleton-free sediments in this section were Subsequently in the Untergrund meadows south of accumulated from 1500 BC to 1000 AD, only 10 % during the sectionsHigh Middle and theAges time (1000 - 1320 AD) periods are shown and insince Figure then, 7. 44 %. The volumes of floodplain sediments concerning HausenDIE ERDE über · Vol. Aar 144 (Fig. · 1/2013 2, No. 5), the authors dated a 43 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Fig. 7 Spatiotemporal quan­ tification of flood­plain sedimentation in the Aar catchment

6. Discussion dle Rhine region. Some ironworks in the region were even shut down temporarily because of the lack of 6.1 The floodplain sediments of the Aar River charcoal. Only a small portion of the remained. Starting in 1856, the factory used fossil hard coal from - the Rhine-Ruhr area (Geisthardt 1957). Another result ment is highly variable, but the total amount is rather of the deforestation was the formation of numerous highThe thickness when compared of floodplain with sedimentsother catchments in the Aar (cf. catch Stolz gullies, concentrated in the wide middle reaches close 2011a; Lang and Nolte 1999). This heterogeneity is to the ancient smelt of Michelbach (Stolz and Grunert the result of different valley forms, varying widths of - sediments is extremely high. Investigations on alluvial ent valley gradients. Thus, in the valleys of the small- fans2006). of some In this gullies area, revealed the thickness remarkably of the rich floodplain skeleton erthe tributaries floodplain thein different young sediments valley sections are thinner and differ and contents, like those of the periglacial coverbeds of the richer of skeleton, due to the larger valley gradients adjacent slopes (Stolz 2008). Therefore, we conclude timeand narrow period mayfloodplains. result in In a verydifferent different valley thickness positions, of that the gully sediments, especially the fine material, a period of and soil erosion for a specific partly reached the Aar floodplain. - these sediments in the Aar catchment is based on the ment properties clearly change. In the lower section of widespreadfloodplain sediments. loess-containing The generally slope deposits high thickness and a long of theWithin Aar athe typical loams floodplain become more profile, clayey. texture This mayand sediindi- history of agriculture, especially in the middle and upper reaches of the valley. Another reason is the se- vere deforestation by small, decentralised ironworks Thecate discoverythat there ofwas whole a very tree slow trunks water (Fig. flow 2 ,on No. the 12) still at during the Middle Ages and one large ironwork dur- thewooded base floodplainof the loams before supports the deforestation this hypothesis. started. The ing Early Modern times. Since 1656 and particularly sandy gravel underneath the trunks indicates that in the 18th century, the iron smelt of Michelbach was there was a higher transport energy of the river during one the largest consumers of charcoal in the Eastern Rhenish Massif. Temporarily, the ironworks of the his- toric Duchy of Nassau employed around 400 people to flood events (snow melt) in the Late Pleistocene and transport the charcoal needed from all over the Mid- Early Holocene. However, without datings, a degree of uncertainty remains with regard to defining the real 44 age of fine gravel underneathDIE the ERDE loamy · Vol. deposits. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Tab. 4 Budgets of the floodplain sediments of the Aar and some other streams in the western German uplands in comparison

6.2 Dating and quantification of sediments In the upper reaches, which were settled later, ­village

Datings in combination with historical facts are time period (-hain/-hahn, -schied and -roth) are common. markers to quantify the sediments. In the Aar catch- Duringnames suffixesthis period, from until the the high-medieval beginning of settlement the Late - Middle Ages at around 1320 AD, 9 million tons of sedi- ment were accumulated in the whole catchment. Af- ment 13 million tons of floodplain sediments were ac terwards, the centralised iron industry of Michelbach Agescumulated in Central during the Holocene (cf. Born until 1989). 1000 TheAD, whichlower can partly be held responsible for around another middleis approximately reaches and the the beginning lower reaches of the of High the Middlecatch- 27 million tons, which accumulated in late medieval ment belong to the earlier settlement phase. Most of and early modern times. Altogether, this value con- the settlements in this region were founded during forms to the calculations of 109.8 mm soil loss in the the Early Middle Ages; their names frequently have -hausen and -heim (Bach 1927). In this case, it is probable to date a large whole Aar catchment outside the floodplain area. - amountthe typical of thesuffixes loams, of which this period: were deposited between 1500 BC and 1000 AD, to the Early Middle Ages and Summarised for the whole catchment, 27 % of over the Franconian colonisation period. Moreover, an in- bank fines were accumulated during the Holocene ­until 1000 AD, 18 % between 1000 and 1320 AD and More55 % betweeninformation 1320 andis needed 1850 AD. regarding the large fluence of prehistoric soil erosion in combination with amount of sediment which was accumulated in the floodplain sedimentation is highly likely, because the- sibleoldest that date the from silty-loamy the base depositsof the overbank in the middle fines near and 1000 AD. Maybe it was partly produced by natural upperHausen reaches refers torepresent the Bronze partly Age. displaced However, late it isglacial pos middle and lower reaches during the Holocene until- - tion must have started in the wide middle and in the plain presumably primary loesses locally exceeding lowerprocesses. reaches Nevertheless, of the Aar thecatchment, floodplain because sedimenta these 6loesses. m were On deposited several whichfoot-slopes was exposedadjacent in to the the excava flood- are the early-settled areas. In the upper reaches over- tion of the construction pit for a shopping centre near Michelbach in November 2010. - bank fines older than from 1000 AD onwards were DIE ERDE · Vol. 144 · 1/2013 not found. The Roman influence is not evidenced al45 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands: though the Romans settled for a short period in the (1.5 t/m² as calculated by Hoffmann et al. 2007), it upper reaches of the Aar to protect the Limes (Baatz is obvious that twice as much skeleton-poor, loamy and Herrmann - - per course could have been eroded before overbank leys of the Nister (12.9 mill. m³ or 19.3 mill. t) and 2002). However, old deposits in the up- thefloodplain Gelbach sediments (15.1 mill. were m³ or stored 22.7 thanmill. t). in The the valdif- lated. Schmenkel (2001) evidenced in the Usa Valley, ference between the Nister and the Gelbach results fines of the High Medieval Ages were even accumu from their different catchment sizes (246 km² and tree p­ollen during the Iron Age, which decreased 221 km² respectively). In the Schwarzbach catchment 30 km east of the Aar, a significant increase of non- (35,1 mill. m³ or 52,7 mill. t), where the bedrock is must have been stronger before Christ. Cereal pollen mostly Bunter , the total quantity of over- couldagain bein theevidenced Roman sinceage. Therefore, the Early Middlehuman Ages.influence The largest proportion of non-tree pollen is proven for the catchment area being four times larger (Stolz 2011b). Schmenkel 2001). bank fines is comparable to that of the Aar, despite the On average, in the Aar catchment at least 11.0 cm or HighBased Middle also on Ages other ( cross-sections which were cored 1647.2 t/ha of areal soil erosion was necessary for de- in the valleys of the Große Nister and the Gelbach (Westerwald) and in the valley of the Schwarzbach Gelbach catchment the values are 7.2 cm or 1,084.5 t/ha, (Palatinate Forest), it was possible to calculate the forpositing the Nister the overbankcatchment fines 5.6 cm to or be 841.8 found t/ha here. and For for the Schwarzbach catchment 3.1 cm or 465.5 t/ha; cf. Tab. 4). amount of overbank fines that was stored in their For­respective each transect floodplain. the average thickness of the over- 6.3 General problems with budgeting soil erosion effects of channels and embankments. Then the data In evaluating these erosion rates, one should keep in bank fines was calculated, in order to eliminate the mind that local extreme weather events and changes As the data can be regarded as being representative in land use are likely to have caused the partial re- ofwere a certain extrapolated reach toof the totalriver, width it was of possible the floodplain. to cal- - culate the total amount for each of the river sections. - The tributaries of the Aar were included in the calcula- sionmoval was of foundoverbank by Schulte fines, andbut Heckmannunconformities (2002) are in difthe tion because of their remarkable sediment input to the ficult to find though. Evidence of such floodplain ero main valley. As referred to above, reasonable estima- tions were made for sections that could not be studied TheHegau distribution loess area of southalluvial western deposits Germany. in a river catch- in detail. The amount of sediment determined was then ment is often not necessarily linear to human impact. compared with the potential erosion area of the catch- - Tab. 4). plain deposition is, in most cases, the exceeding of aThe critical crucial threshold factor for in startingsoil erosion an increasing(Hoffmann floodet al. Thisments result (catchment complies size with minus our floodplain results from area; the Große 2010). Smaller former erosion events can only be de- north of the Aar, from the younger settlement phase, Nister catchment in the High Westerwald Mountains, tected by Holocene colluvia along the slopes. from the late medieval to the modern age. The av- variable amongst several for budgeting soil erosion eragewhere value 55 % of of soil the erosion overbank in finesthe Nister were catchment deposited withinThus, the a catchment. amount of Other floodplain factors deposits are: the is degree only one of amounts to 56.1 mm and in the adjacent Gelbach catchment to 72.3 mm (Stolz 2011a). In contrast, Lang colluvial sediment storage at the slopes, local alluvial and Nolte (1999) dated most of the young overbank fanstruncation and the of output soil profiles from the within catchment. the catchment, It is, however, the - AD, which shows that the loess-rich Wetterau depres- uring the erosion rate of the slopes more information sion,fines asof thepart Wetter of the RiverRhine-Main at between lowlands, 700 AD was and settled 1000 difficult to measure or to calculate these. For meas much earlier than the upland regions. needed (cf. Förster and Wunderlich 2009). In a similar way,about the the measuring original thickness of the colluvia of those volume soil profilesis compli is- In the Aar Valley with more than 32 mill. m³ of sedi- cated because geological and pedological maps are ment volume, equivalent to almost 50 mill. tons unusable in most cases (cf. Moldenhauer et al. 2010,

46 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Seidel and Mäckel 2007). Furthermore, the thickness for Early Modern Times, triggered by deforestation in of colluvia is very variable. This study focuses only connection with the local iron industry. The calculated

soil erosion of 11 cm in the whole catchment. derived.on the floodplain This value sediments. is calculated From to these, 11 cm a inminimum the Aar total amount of overbank fines correlates to an average catchmentvalue for the and, average in contrast, truncation 3.1 cm of in soil the profiles more recently can be As a result, the example from the Aar River demon- populated and densely forested Schwarzbach catch- ment (Palatinate Forest; Tab. 4; Stolz 2011b). Seidel man in the uplands of Central Europe with drastic and Mäckel (2007) tried to calculate the total erosion consequencesstrates that there for the were landscape. strong influences of historic for the Elz () and the Möhlin catchments (Breisgau, southwest Germany, partly with prehis- toric settlements) to 31-61 cm, respectively 44-79 cm. Acknowledgement These high values are three to seven times higher than those from the Aar catchment. Therefore, a much high- The authors wish to thank Prof. Dr. Detlef Busche † for er amount of total erosion would be plausible. For the Aufsess catchment (Upper Franconia, Bavaria) Fuchs open questions. his help translating the paper and finding answers to threeet al. (2010) times havethe amount budgeted of onlyalluvial 9% alluvialsediments. sediments In the 8. References Geuland 33% River catchment catchment output. (southern Here Netherlands) the output is De nearly Moor and Verstraeten Ad-hoc AG Boden 2005: Bodenkundliche Kartieranleitung. – 5. Auf­ lage. – Stuttgart (2007) calculated more than 80% of Anderle, H.-J. 1991: Erläuterungen zur geologischen Karte, Blatt Ages.colluvium, During and the only time 13%before, of the alluvial main sedimentspart of the sedi have- mentsbeen stored was exported in the catchment out of the catchment. since the High Middle Wiesbaden 5715, Idstein. – Hessisches Landesamt für Bodenforschung. – Andres, W. 1967: Morphologische Untersuchungen im Limburger To sum up, the results provide evidence for much high- Becken und in der Idsteiner Senke. – Rhein-Mainische Forschun- er values concerning areal historic soil erosion and gen 61. – Frankfurt the formation of alluvial sediments in Central Euro- Bach, A. 1927: Die Siedlungsnamen des Taunusgebiets in ihrer pean Uplands than was realised until now. Therefore, Bedeutung für die Besiedelungsgeschichte. – Rheinische Sied- lungsgeschichte 1. – Bonn Central Europe were truncated by several decimetres Baatz, D. und F.-R. Herrmann duringmost of historic the soil and profiles pre-historic in the cultural periods. landscapes of Blume, H.-P. - 2002: Die Römer in Hessen. – Stuttgart minologie, Verfahrensvorschriften und Datenblätter; physika- (Hrsg.) 2000: Handbuch der Bodenuntersuchung. Ter lische, chemische, biologische Untersuchungsverfahren; gesetz­ 7. Conclusions liche Regelwerke. – Loseblattsammlung. – et al. Bork, H.-R. und A. Kranz In the catchment of the Aar River, 48.8 mill. tons of prägt Deutschland. Neue Forschungsergebnisse aus dem Ein- 2008: Die Jahrtausendflut des Jahres 1342 loamy, downwards increasingly sandy or clayey over- zugsgebiet des Mains. – Jahresberichte der Wetterauischen Ge- sellschaft für die gesamte Naturkunde 158: 119-129 5.0 m thick, which is a very high value for a small catch- Bork, H.-R., H. Bork, C. Dalchow, B. Faust, H.-P. Piorr und T. Schatz mentbank of fines 312 are km². stored Sometimes in total. isolated The loams gravel are layers 1.5 or to 1998: Landschaftsentwicklung in Mitteleuropa. Wirkungen des Menschen auf Landschaften. – Gotha observed. The anthropogenically triggered sedimen- Born, M. 1989 : Die Entwicklung der deutschen Agrarlandschaft. – tationsmall sand-filledbegan in the streams lower middle within and the lower loams course could auf be 29. – Darmstadt the Aar River at the earliest during the Bronze Age. A Brosche, K.-U. 1984: Zur jungholozänen und holozänen Entwicklung 2. Auflage. – Erträge der Forschung small proportion may have been deposited even earlier, - 34 (1): des Werratals zwischen Hannoversch-Münden und Philippsthal tion did not begin before 1000 AD, even though the 105-129 (östl. ). – Eiszeitalter und Gegenwart Romansof natural had origin. already In the settled upper in course, this mountainous first sedimenta area. Coulthard, T.J., M.G. Macklin and M.J. Kirkby 2002: A cellular model of

Surface Processes and Landforms 27 (3): 269-288 The strongest sedimentation intensity (55 % of the Holocene upland river basin and alluvial fan evolution. – Earth overbankDIE ERDE fines· Vol. 144in the · 1/2013 whole catchment) was evidenced 47 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

De Moor, J.J.W. and G. Verstraeten 2008: Alluvial and colluvial sedi- Hövermann, J. 1953: Studien über die Genesis der Formen im Tal­ ment storage in the Geul River catchment (the Netherlands). grund südhannoverscher Flüsse. – Nachrichten der Akademie der Wissenschaften Göttingen 1. – Göttingen sediment budget. – Geomorphology 95 (3-4): 487-503 Hoffmann, T., G. Erkens, K.M. Cohen, P. Houben, J. Seidel and R. Dikau combining field and modelling data to construct a late Holocene Dietz, T. 1968: Die würm- und postwürmglazialen Terrassen des - Lech und ihre Bodenbildungen. – Eiszeitalter und Gegenwart 17 (1): 105-118 2007: Holocene floodplain sediment storage and hillslope ero 19: 102-128 Hoffmann, T., A. Lang and R. Dikau sion within the Rhine catchment. – The Holocene Dotterweich, M. - analysing 14 - 2008: Holocene river activity: posits in small catchments of central Europe: deciphering the many. – Science Reviews 27 (21-22): 2031-2040 2008: The history of soil erosion and fluvial de C-dated fluvial and colluvial sediments from Ger long-term interaction between humans and the environment – Hoffmann, T., G. Erkens, R. Gerlach, J. Klostermann and A. Lang 2009: a review. – Geomorphology 101 (1-2): 192-208 Dreibrodt, S., C. Lubos, B. Terhorst, B. Damm and H.-R. Bork 2010: the Rhine catchment. – Catena 77(2): 96-106 Trends and controls of Holocene floodplain sedimentation in Hoffmann, T., V.R. Thorndycraft, A.G. Brown, T.J. Coulthard, B. - chronology, research perspectives. – Quaternary International nati, V.S. Kale, H. Middelkoop, B. Notebaert and D.E. Walling 2010: Historical soil erosion by water in Germany. scales and archives, 222 (1-2): 80-95 - Förster, H. und J. Wunderlich Human impact on fluvial regimes and sediment flux dating dur upland catchments. the problem of soilscape model and data and Planetary Change 72: 87-98 2009: Holocene sediment budgets for ing the Holocene: review and future research agenda. – Global availability. – Catena 77 (2): 143-149 Houben, P., T. Hoffmann, A. Zimmermann and R. Dikau 2006: Land Fuchs, M., M. Fischer und R. Revermann 2010: Colluvial and al- use and climatic impacts on the Rhine system (RheinLUCIFS): luvial sediment archives temporally resolved by OSL dating: implications for reconstructing soil erosion. – Quaternary data. – Catena 66 (1-2): 42-52 quantifying sediment fluxes and human impact with available ­Geochronology 5 (2-3): 269-273 International Union of Soil Sciences 2006: World reference base Fuchs, M. and G.A. Wagner bleaching by small aliquots of quartz for reconstructing soil correlation and communication. – 2. ed. – World Soil Resources 2003: Recognition of insufficient for soil resources: a framework for international classification, erosion in Greece. – Quaternary Science Reviews 22 (10-13): Reports 103. – Rome 1161-1167 Jacomet, S. und A. Kreuz 1999: Archäobotanik: Aufgaben, ­Methoden Galbraith, R.F., R.G. Roberts, G.M. Laslett, H. Yoshida and J.M. Olley und Ergebnisse vegetations- und agrargeschichtlicher 1999: Optical dating of single and multiple grains of quartz from Forschung. – Stuttgart Jinmium rock shelter, northern Australia: part I, experimental Jain, M., A. S. Murray and L. Bøtter-Jensen 2004: Optically stimu- design and statistical models. – Archaeometry 41 (2): 339-364 Gautier, E., J. Corbonnois, F. Petit, G. Arnaud-Fassetta, D. Brunstein, 15: 143-157 lated luminescence dating: how significant is incomplete light S.Grivel, G. Houbrechts and T. Beck 2009: Multidisciplinary ap- Kleber, A. 1997: Cover-beds as soil parent materials in midlatitude exposure in fluvial environments? – Quaternaire regions. – Catena 30 (2-3): 197-213 Géomorphologie: Relief, Processus, Environnement 2009 (1): Klimek, K., M. Lanczon and J. Nogaj-Chachaj - proach for sediment dynamics study of active floodplains. – 65-78 tion as a cause of alluvium in small valleys, Subcarpathian loess 2006: Historical deforesta Geisthardt, F. 1957: Landesherrliche Eisenindustrie im Taunus. – , . – Regional Environmental Change 6: 52-61 Nassauische Annalen 68: 156-174 Koch und E. Kayser Händel, D. 1969: Auelehmsedimentation und Laufentwicklung in 1:25000. Blatt 5614 (Limburg). – In: Geologische Karte von 1886: Geologische Spezialkarte von Hessen den Auen der Weißen Elster und Pleiße (Westsachsen). – Peter- manns Geographische Mitteilungen 113 (1): 16-20 anstalt. – Berlin Hessen. – with comments. – Preußische Geologische Landes­ Hempel, L. 1976: Bodenerosion und Auelehm. – In: Richter, G. Koch, C. und E. Kayser 1881: Geologische Spezialkarte 1:25000. Blatt

430 comments. – Preußische Geologische Landesanstalt. – Berlin (Hrsg.): Bodenerosion in Mitteleuropa. – Wege der Forschung 5714 (Kettenbach). – In: Geologische Karte von Hessen. – with Heusch, K., J. Botschek und A. Skowronek 1996: Zur jungholozänen Lang, A. and S. Nolte . – Darmstadt: 331-333. – first published 1957 sedi ­ments from the Wetterau, Germany, provided by optical 1999: The chronology of Holocene alluvial Mäanderbogen. – Eiszeitalter und Gegenwart 46: 18-31 and 14 9 (2): 207-214 Oberflächen- und Bodenentwicklung der Siegaue im Hennefer Hildebrandt, H., B. Heuser-Hildebrandt und M. Stumböck 2001: Be- Mäckel, R. 1970: Untersuchungen zur jungquartären Fluss­ C dating. – The Holocene standsgeschichtliche und kulturlandschaftsgenetische Unter­­­ geschichte der Lahn in der Gießener Talweitung. – Eiszeitalter suchungen im Naturwaldreservat Stelzenbach, Forstamt Nas- und Gegenwart 20: 139-173 sau, Revier Winden: Pollenanalyse aus Geländemulden und Mäckel, R. und A. Friedmann

1999: Holozäner Landschaftswandel Mainzer Naturwissenschaftliches Archiv. – Beiheft 25 alter und Gegenwart 49: 1-20 Auswertung von Holzkohlespektren historischer Meilerplätze. – im südlichen Oberrheintiefland und Schwarzwald. – Eiszeit­

48 DIE ERDE · Vol. 144 · 1/2013 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Mensching, H. 1951: Akkumulation und Erosion niedersächsischer J. van der Plicht, C.E. Weyhenmeyer 2009: IntCal09 and marine09 Flüsse seit der Risseiszeit. – Erdkunde 5: 60-70 radiocarbon age calibration curves, 0-50,000 years cal BP. – Moldenhauer, K.-M., J. Heinrich and A. Vater 2010: Causes and h­ istory ­Radiocarbon 51 (4):1111-1150 of multiple soil erosion processes in the northern up- Rother, N. lands. – DIE ERDE 141 (3): 171-186 Nordostabdachung des Sollings (Südniedersachsen). – Göttinger 1989: Holozäne fluviale Dynamik im Ilmetal und an der Mühr, B. (2007): Klimadiagramme weltweit. – online available at: Geographische Abhandlungen 87 www.klimadiagramme.de, 15/07/2012 Sauer, D. and P. Felix-Henningsen 2006: Saprolite, soils and sedi- Munsell Color Company (ed.) 1990: Soil color charts. – Baltimore ments in the Rhenish massif as records of climate and landscape Murray, A.S. and A.G. Wintle 2000: Luminescence dating of quartz history. – Quaternary International 156-157: 4-12 using an improved single-aliquot regenerative-dose protocol. – Schirmer, W., J.A.A. Bos, R. Dambeck, M. Hinderer, N. Preston, A. Radiation Measurements 32: 57-73 Schulte, A. Schwalb and M. Wessels - Natermann, E. 1941: Das Sinken der Wasserstände der Weser und cesses and valley history in the river Rhine catchment. – Erd- 2005: Holocene fluviatile pro ihr Zusammenhang mit der Auelehmbildung des Wesertals. – Ar- kunde 59 (3): 199-215 chiv für Landes- und Volkskunde Niedersachsen 1941: 288-309 Schmenkel, G. 2001: Pollenanalytische Untersuchungen im Tau- Neumeister, H. 1964: Beiträge zum Auelehmproblem des Pleiße- nus. – Berichte der Kommission für Archäologische Landes- und Elstergebietes. – Wissenschaftliche Veröffentlichungen des 6: 225-232 Instituts für Länderkunde. – N.F. 21/22: 65-131 Schulte, A. and T. Heckmann forschung in Hessen Niller, H.P. 2001: Wandel prähistorischer Landschaften. Kollu- 2002: Human influence on Holocene vien, Auelehme und Böden. Archive zur Rekonstruktion vor- Zeitschrift für Geomorphologie. – Beiheft 128: 67-79 environmental change in the Hegau region, SW Germany. – geschichtlicher anthropogener Landschaftsveränderungen im Schweingruber, F.H. 1990: Microscopic wood anatomy. structural Lössgebiet bei . – Erdkunde 55: 32-48 variability of stems and twigs in recent and subfossil woods Pörtge, K.-H. und P. Molde 1989: Feststoff- und Lösungsabtrag im from central Europe. – 3rd edition. – Birmensdorf Einzugsgebiet des Wendebachs. – Göttinger Geographische Ab- Seidel, J. and R. Mäckel handlungen 86: 115-122 river catchments in the southern valley. – Geomor- 2007: Holocene sediment budgets in two Pott, R. phology 92 (3-4): 198-207 lage. – Stuttgart Seidenschwann, G. 1989: Zur jungpleistozän-holozänen Entwick- 1995: Die Pflanzengesellschaften Deutschlands. – 2. Auf­ Prescott, J.R. and J.T. Hutton 1988: Cosmic ray and gamma ray do- lung der Kahl. – Frankfurter Geowissenschaftliche Arbeiten simetry for TL an ESR. – Internatio‑‑­al Journal of Radiation 10: 17-30 Applications and Instrumentation. Part D. Nuclear Tracks and Semmel, A. 1968: Studien über den Verlauf jungpleistozäner For- Radiation Measurements 14 (1-2): 223-227 45. – Prescott, J.R. and J.T. Hutton 1994: Cosmic ray contributions to Frankfurt mung in Hessen. – Frankfurter Geographische Hefte dose rates for luminescence and ESR dating: large depth Stolz, C. and long-term time variations. – Radiation Measurements der Aar zwischen Wiesbaden und Limburg. – Geologische Ab- 2008: Historisches Grabenreißen im Wassereinzugsgebiet 23 (2-3): 497-500 117. – Wiesbaden Pretzsch, K. 1994: Spätpleistozäne und holozäne Ablagerungen als Stolz, C. handlungen Hessen - the central Rhenish mountains (Westerwald), Germany. – 2011a: Budgeting soil erosion from floodplain sediments of tleren Leine. – Göttinger Geographische Abhandlungen 99: 29-72 21 (3): 499-510 Indikatoren der fluvialen Morphodynamik im Bereich der mit Raab, T., K. Hürkamp and J. Völkel 2010: Stratigraphy and chronol- Stolz, C. 2011b: Budgeting soil erosion from floodplain and The Holocene alluvial fan sediments in the Forest area, Vils river valley, east Bavaria, Germany. – Physical Geo­ (Pfälzerwald, Germany). – Zeitschrift für Geomorphologie, ogy of late quaternary floodplain sediments in a historic mining graphy 28: 357-384 N.F. 55 (4): 437-461 Raab, T., S. Beckmann and N. Richter 2005: Reconstruction of Stolz, C. 2011c: Spatiotemporal budgeting of soil erosion in the

study. – DIE ERDE 136 (1): 47-62 (Taunus Mts., Western Germany). – Erdkunde 65 (4): 355-370 floodplain evolution in former mining areas. the Vils river case abandoned fields area of ‘Rahnstätter Hof’ near Michelbach Reichelt, G. 1953: Über den Stand der Auelehmforschung in Stolz, C., J. Grunert and A. Fülling 2012: The formation of alluvial Deutschland. – Petermanns Geographische Mitteilungen 97: 245-261 ­Eifel mountains, western German uplands: a study of soil ero- fans and young floodplain deposits in the Lieser catchment, Reimer, P.J., M.G.L. Baillie, E. Bard, A. Bayliss, J.W. Beck, P.G. Blackwell, 22 (3): 267-280 C. Bronk-Ramsey, C.E. Buck, G.S. Burr, R.L. Edwards, M. Friedrich, Stolz, C. and J. Grunert - sion budgeting. – The Holocene P.M. Grootes, T.P. Guilderson, I. Hajdas, T.J. Heaton, A.G. Hogg, scape history of the central Palatinate Forest (Pfälzerwald, 2010: Late Pleistocene and Holocene land K.A. Hughen, K.F. Kaiser, B. Kromer, F.G. McCormac, S.W. Manning, South-Western Germany). – Quaternary International 222: R.W. Reimer, D.A. Richards, J.R. Southon, S. Talamo, C.S.M. Turney, 129-142

DIE ERDE · Vol. 144 · 1/2013 49 a case study from the Aar Valley in the southern Rhenish Massif, Germany Quantification and dating of floodplain sedimentation in a medium-sized catchment of the German uplands:

Stolz, C. and J. Grunert 2008: Floodplain sediments of some streams Thomas, J. in the Taunus and Westerwald mts., western Germany, as evi- morphodynamik an der oberen Oberweser. – Göttinger Geogra- 1993: Untersuchungen zur holozänen fluvialen Geo­ dence of historical land use. – Zeitschrift für Geomorphologie. – phische Abhandlungen 98. – Göttingen N.F., 52 (3): 349-373 Tinapp, C., H. Meller and R. Baumhauer - Stolz, C. and J. Grunert - tion of colluvial and alluvial sediments in the Weiße Elster river 2008: Holocene accumula mation and historical land use. a case study from the Taunus valley in Saxony, Germany. – Archaeometry 40 (4): 696-709 2006: Holocene colluvia, medieval gully for mountains, southern Rhenish slate massif. – Zeitschrift für Geo- Urz, R. 2003: Die jungpleistozäne Talfüllung der mittleren Lahn. morphologie. – N.F., Beiheft 142: 175-194 Ein Spiegel der kaltzeitlichen Klimaschwankungen im hes- Stuiver, M., P.J. Reimer, E. Bard, J.W. Beck, G.S. Burr, K.A. Hughen, sischen Mittelgebirge. – Zeitschrift für Geomorphologie N.F. B. Kromer, G. McCormac, J. van der Plicht and M. Spurk 1998: 47 (1): 1-27 IntCal98 radiocarbon age calibration, 24,000–0 cal BP. – Wallinga, J. - ­Radiocarbon 40 (3): 1041-1083 vial deposits: a review. – Boreas 31 (4): 303-322 2002: Optically stimulated luminescence dating of flu

50 DIE ERDE · Vol. 144 · 1/2013