River history of the Great Lauter

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South-west German layer level country , almost riveless Swabian Alb due to karstification

The flow history of the Great Lauter Like the other recent Albflüsse a geologically very long, eventful development behind it. Only a few, very old, formerly very large bodies of water in the Swabian Alb still transport their water and sediment loads above ground to their confluence with the Danube.

The original versions of the large bodies of water, now more streams and small rivers, came from the northern foothills of the Alb or at least crossed the then larger area, which is commonly defined as the "Alb table". Most of these former primary rivers still cross the Swabian Alb from north to south-east. A few tracks are understandable to the untrained eye, like the most today Albtrauf observable Strunk passports .

Preliminary remark

The publication by Fahlbusch (1981) Miocene and Pliocene - What is what? initiated a massive change in the stratigraphic structure of the Neogene (Miocene, Pliocene) for southern Germany in geology. (Adaptation to an internationally standardized classification). Since evidence is used here that was published before this caesura, it was adapted to the stratigraphy that is valid today. The adaptation (serial specification Miocene or Pliocene) is in individual cases u. U. was not hit accurately enough.

Fluvial sedimentation by primary rivers from the north

Southwest Germany in the Miocene

Since 1931, the most important evidence of ancient rivers coming from the north are Miocene sediment relics . If these sediments are coarse-grained, baked rocks, they are included in the category of conglomerates , which, if they come from the Alps, are called Nagelfluh. The term “Juranagelfluh” has become established for the equivalent of river sediments from the north. From the composition, age, location and distribution of such sediments "some concrete indications can be derived about the Upper Miocene river network of the northern foothills of the Alb and the Alb." Breg and Brigach belong to both today and then important flowing waters from the north (from west to east) , Faulenbach (remnants of a mighty primeval Eschach draining the Black Forest ), Bära , Schmiecha / Schmeie, Fehla / Lauchert , Große Lauter and Brenz . Insignificant today, Ur- Lone and Ur- Eyb were as important as the other rivers mentioned.

Danubian Große Lauter tapped by the "Rhenish" Echaz (today 7.9 km dry valley to the source)
Graupensandrinne , Younger Juranagelfluh on the Hegaualb

In geological maps and in graphics and text contributions Juranagelfluh deposits are noted between the Randen ( Klettgau also) in the Westalb and the great-Eyb / Lone ( "Couch Heimer strand") on the Ostalb even after millions of years as a geological archive remains noted are. Uplifting processes in the Black Forest and the sloping of the Alb plateau to the south-east allowed primeval rivers from the Black Forest to pour by far the largest amounts of sediment Jüngere Juranagelfluh (total thickness up to 380 m). The Jüngere Juranagelfluh, which was poured into four gullies (Tengener, Geisinger, Bittelbrunner and Emminger gullies) between Tengen and Emmingen (west-east) in the West Alb initially only cut through the Albsteinplatte, emptied into the wide, flat barley sand channel and filled it. The quantities were so huge that during the Middle Miocene the entire Albstein area up to the top of the cliff and the barley sand channel was locally filled with Juranagelfluh.

River pebbles of the younger Juranagelfluh in the former quarry near the village of Hondingen , Hegaualb
River pebbles from the Younger Juranagelfluh still cover fields on the Hegaualb today

The Juranagelfluh pebbles, the high tertiary age of the still existing rivers named above, only form a thin layer or even consist only of scattered gravel. In one case it is only relics in a tuff vent that was active in the Miocene . The fillings of the Younger Juranagelfluh were therefore only in a limited area of ​​the western Alb, thick deposits that even buried the barley sand channel and the landscape north of it.

When looking back at the history of the river network in the Miocene, one must also consider the Alb plateau as a whole and it is essential to include the time before the "Danube drainage channel" was formed (long Miocene period before the Upper Miocene). Here a barley sand channel up to 13 km wide and on average approx. 60–80 m deep with a slight gradient directed to the south-west (!) Dominated the northern edge of the Molasse basin . The primeval rivers flowed into this barley sand channel before the Urdonau emerged in the Upper Miocene. The primary rivers from the north delivered their cargo via the barley sand channel to the southwest into a residual sea in the Swiss plateau . After the erosion phase , layers of sand were deposited in the channel, but the existing sediments of the last Molasse Sea (Lower Miocene of the Upper Sea Molasse, OMM) and, in some cases, also the underlying river sediments of the Lower Freshwater Molasse (USM) of the Molasse Basin were removed. So much sediment material (above all Upper Freshwater Molasse, OSM) was delivered from the Alps that these fillings completely filled the barley sand channel along its entire length. Today the gutter is morphologically no longer perceptible.

In the Miocene, the entire Alb was buried up to 70 m high by the alpine freshwater molasse (OSM), so that the channels in the lower reaches of the north were temporarily sealed. On the southern Middle Alb, tertiary sediments (especially upper freshwater molasses) have not yet been completely eroded everywhere ( Tautschbuch , Emerberg, Landgericht , Hochsträß ).

In the Miocene, the climate gradually began to cool from subtropical to warm-temperate conditions. During this long period, however, there were multiple changes between humid and arid periods.

The Predanubic and the Danubian Urlauter

The existence of the Miocene Jüngerer Juranagelfluh was documented by Skull (1973) in the Hungerberg tuff chimney (near Münsingen ). The pebbles deposited far above today's land surface had fallen back into the chimney as the volcanic activity subsided . Kiderlen (1931) saw grit in "hanging parts of the Alenberg north of Hayingen and in the OSM of the Emerberg". He assigns this to a Urlauter. Prinz (1959) occupies Juranagelfluh in the “Bising” district, approx. 1.7 kilometers by road east of Oberwilzingen , southwest of today's Lauter. (Well-rounded pebbles on a Bisingen field, which can be such river pebbles, are shown in the photo "Bising finds").

Example of a body of water dominated by rubble , gravel and coarse sand of various sizes
River gravel , younger Juranagelfluh, fluvial sediment , Miocene Urlauter, "Bising" ( Oberwilzingen )

The course and character of this original river is a flat, very broad, hardly deepened, north-south directed river - similar to the early Aaredonau (see below). The Urlauter was a powerful original river in the Miocene, but was rather small in relation to the Juranagelfluh rivers flowing over the western Alb. Those of the western Alb had their catchment area not only from the Alb table, which at that time extended further to the northwest, but also from the northern foothills of the Alb and even the Black Forest. The valley of the Ur-Lone lay between the Upper Miocene Albstufenrand and today's eaves of the Middle Alb. As a large, water-rich forerunner of the Lone, this Danubian Ur-Lone attracted all fluvial catchment areas near the edge of the Alps. The relief traces of the Ur-Lone and its tributaries have long since disappeared with the relocation of the Alb eaves and the further development of the northern foothills of the Alb. The LGRB has given a graphic of the original rivers coming from the north and their more recent river versions that flowed into the Upper Danube (cf. the graphic image "Danube development, Miocene until today"). Geographically, the Urlauter would have flowed into the Graupensandrinne near Lauterach , and then after the formation of the Urdonau into the early Urdonau (Aaredonau).

Danube development and most important tributaries from the north, Miocene until today

Danube development, first karstification, first deepening of the Great Lauter

Southwest Germany in the Pliocene

The sustained sinking of the Upper Rhine Rift from the Upper Miocene initiated the second major tectonic phase in southwest Germany. The Black Forest was raised and the ceilings removed down to the basement . A considerable tectonic tipping of the Swabian Alb (elevation of the layers into steps and inclination from west to east enabled the origin and development of the primeval Danube .) The very mighty Aaredonau drained the western Alps (Switzerland) and flowed over today's Lower Wutach valley and the dry valley of the Aitrach in sluggish, heavily overgrown, kilometer-wide gullies on the Alb to the east, clearing the molasse sediments that were still widespread at that time . This early Aaredonau might have looked something like the middle part of the last unregulated river Tagliamento still to be found in Central Europe , Italian Southern Alps (see the photo Tagliamento).

Urdonau-like: The last still unregulated river " Tagliamento " in Central Europe (Italian Southern Alps)

The northern primary rivers were also still under the huge alpine OSM sealing of the Alb. The uplift and tilting of the southern German large floe led to the fact that its rivers gradually cut from the Pliocene onwards, the burial material (the "sealing") gradually cleared out again and the relief also changed further.

The original rivers poured their river cargo (water and Juranagelfluh) no longer into the Graupensandrinne or the Molasse basin, but now into the Urdonau.

The great original Danube became the dominant drainage line. This shaped the developing water system of the greater part of the still extensive flat southern German layer level country up to the Middle Pliocene. The Aaredonau / Danube is undisputedly occupied by a number of remnants of Pliocene Danube hill gravel - between Blumberg and Ulm on the Alb and then also sporadically. On the Middle Alb, this wide Danube came within two kilometers of the cliff line. However, the diversion of the Aare to Doub / Saone / Rhone weakened the Aaredonau, 6/7 of the water volume was lost to the Danube. The Alpine Rhine flowed through Upper Swabia near Ehingen into the Danube until the oldest Pleistocene .

The Aaredonau / Danube reached its main stage of deepening by the end of the Pliocene. “At its end the river already had a 150 m deep box valley. During the Ice Age, only 50 m of today's valley depth were created (...). "

The all-important river history events on the Miocene / Pliocene border were:

  1. The second great tectonic phase; the sinking of the Upper Rhine Graben with the ensuing weakening of the northern primary rivers (including the Juranagelfluh channels in the Hegau) due to regressive erosion and tapping of tributaries (Black Forest from Upper Miocene and above all, Neckar in the foothills of the Alps)
  2. The "Amputation" Wagner (1961) of the Aaredonau due to the loss of diversion of the water masses in the Middle Pliocene
  3. Swabian Alb: uplift (inclination from north to south), tilting (to the east) and adjustment of all waters to these consequences and with it the gradual devastation and karstification (which is based on the receiving water , the deeply deepened Danube)

Up until the Middle Pliocene, the current main valley systems, which drained to the Danube and thus the bas-relief of the southern German layer level country, were “fixed” throughout southern Germany. In its history, the Danube has shifted its course to the south several times, as evidenced by the spread of the “Pliocene Danube hill gravel”. The dismantling of the Alb eaves, mainly due to the receding erosion of the Neckar and its tributaries (consequence of the sinking of the Upper Rhine Valley) followed. The karstification developed into deep karstification in such a way that the tributaries of the large drainage channels (to the Danube) at different times gradually dried up at least in their upper and middle reaches and hardly supplied water to the large channels.

The Danubian Great Lauter

After the formation of the original Danube and the massive changes in the Danube, the Große Lauter gradually cut its way, but - like the entire river system of the Alb plateau - always aligned with the course of the Danube.

Night eaves and catchment areas of the Supreme Great Lauter

Branco (1884) found the White Jura in various Swabian volcanoes , which were active during the Alb volcanism (Lower to Upper Miocene). In the Scharnhausen chimney (9 km southeast of Stuttgart), around 20 km north of today's Albtrauf, he found Oxford limestone, as well as in the Georgenberg volcanic chimney, south of Reutlingen. Even in the Pliocene, the Albtrauf was a few kilometers further north than it is today (dates are only given in the Pleistocene, see below). The Pliocene Alb plateau up to the eaves at that time and thus the northern catchment area of ​​the Danube tributaries of the Middle Alb was considerably larger than today.

The Albtrauf , which is ragged today , view from the Roßberg to the southwest

It is disputed which of the main valley branches of the Pliocene Lauter were in front of and behind the earlier eaves. The very deep penetration of the Echaz eaves bay has destroyed all young tertiary surfaces and made the role of the side valleys on both sides of the eaves bay difficult to interpret. Of the mostly completely dry feeders to the now dry upper reaches of the Lauter, 8 valleys can be identified, including several that joined before the confluence with the now dry Lauter upper reaches. There are considerable height differences between today's Alb foreland and these Danubian tributaries and the Lautertal, which can be easily recognized on today's Albtrauf as so-called Strunk Passes with height differences of 100 to 200 m. Here one must assume an early "Rhenish intervention" (retrograde erosion at the Rhine, Neckar and Echaz), which is based on the Upper Rhine Rift, which has developed since the Miocene. The “aggressiveness” of the Rhine results from the considerably greater gradient of the Rhine to the North Sea than the gradient of the Danube to the Black Sea.

Deepening and first deep karstification of the Great Lauter in the Pliocene

Flat dry valley , Große Lauter near Kohlstetten in the Plio-Pleistocene

The mass limestone, a non-stratified White Jura, is harder than stratified White Jura due to its biogenic nature and is therefore much more resistant to deepening through erosion. While the upper course is wide and flat, from Hundersingen the Lautertal suddenly narrows to a partially gorge-like rock valley. On its way to the confluence with the Danube, the Große Lauter must for the most part deepen in the mass limestone of the Lower and Upper Rock Limestone formations. The change between the narrow rock and the wider valley can be observed several times over the 44 km of today's river length. In a longitudinal section drawing, Prinz (1959) shows for today's Große Lauter that although the slope of the river valley fluctuated, it had to be 33% greater on the last 20% of the course! Only in this way could the confluence with the rapidly deepened receiving waters of the Danube succeed. This proves that the deepening of the Great Lauter in the hard mass limestone progressed only slowly and more slowly than the deepening of the Danube.

"In the Pliocene, the climate cooled significantly compared to the earlier Tertiary and already showed fluctuations similar to those typical for the Quaternary." Abel (2003) p. 152. Abel was able to deepen this finding, which is well documented in global climate research connect the valleys of the Middle Alb.

Pleistocene to date

The size of the catchment area of ​​the Upper Lauter always depended on how far the Danubian Ur-Lone and then the Rhenish river system allowed it. With the elevation of the strata of the Jura and the relocation of the night eaves back through removal, the question arises of where the night eaves was and when. With the Scharnhauser volcanic vent of the Miocene system of the Swabian volcano, there was a first usable time stamp (Branco 1884, see above). How far was the Alb eaves relocated back and thus the northern Alb plateau removed? A temporal classification of the decline in eaves was estimated for the oldest Pleistocene to be 5 km before today. In the Young Pleistocene (Riss period) 2 km before today. In the abandoned Neckar valley loop of the Odenwald near Mauer, Juragerolls were found. Accordingly, the Rhine-Neckar tributary Echaz was already immersed in the Jura of the Swabian Alb in the Middle Pleistocene ( Cromer complex or earlier).

Recess levels and terrace strips

Stations in the deepening of a river by water erosion ( terrace formation)

Both the Pliocene and the Pleistocene valley depressions did not take place in one go. In all of the larger valleys of the Alb Felsterrassen there are indentations . Have there been phases of stagnation in the development of the deepening since the first deepening of the Great Lauter (or Urlauter)? Remaining relics of the lowering of the Lauter are in the form of terrace steps. For the development of the Pleistocene deepening, rocky terraces (not embankment terraces) were found on the dry and water-bearing Lauter upper reaches to Hundersingen and again for the non-rocky narrow valley sections of the Middle Lauter between Derneck Castle , Indelhausen and Anhausen, which probably belong to different valley floor levels. Terraces of the level around 20 m above today's valley floor are clearly defined. They are still at the base of the valley widening and are often used for agriculture. Boulders on the terraces can only be found sporadically in the Middle Alb. Ablation processes, such as B. cold-age solifluction flow , terraces may have overprinted.

Extreme climatic fluctuations: ice ages, interglacials, warm periods

In the Upper Miocene, fluctuations in temperatures and precipitation had already set in. These fluctuations increased in the Pliocene and then in the Pleistocene. In the Middle Pleistocene, the climate was already so cyclical that Berger et al. (1994) speak of the 'Middle Pleistocene Revolution'. On the Swabian Alb, these strong climatic fluctuations made themselves felt in the frequent alternation between erosion and sedimentation. After the Pliocene, the Danube deepened for the last 50 m. The Lauter finally had to delve into this level. With the remaining deepening of the Lauter, the level of the karstification has gradually settled at this level of the Danube. By then, at the latest, the last side valleys of the Great Lauter and their own upper course had finally completely dried up! During the greatest climatic fluctuations, the erosion base of the Danube had more or less reached its present level. This process and the creation of the mature subterranean karst system were essentially completed before the strongest cyclicality began.

In the cold ages of the Mindel, Riss and Würm complexes, i.e. at the time of the strongest cyclicality, the karst of the Swabian Alb was, however, continuously in the periglacial area . The karstification ability was reduced, in winter months permafrost can also have sealed large parts of the river system so that snowmelt or rain precipitation could not seep down into the dry or water-bearing valleys. Persistent above-ground removal of precipitation naturally widened the valley profile again.

Course changes, tectonic disturbances

Umlaufberg der Große Lauter, 100 m impact slope , juniper heather on the right flank

The Lautertal is wide and flat in the upper reaches, rocks appear to the south and narrow the valley to a partially gorge-like rock valley. Then the Lautertal expands again temporarily. The Mittelberg breakthrough mountain protrudes south of Hundersingen. Here the Lauter has shortened the narrow valley of a side stream. Further down the valley, Unterer Massenkalk has forced the deepening of an ancient, large meander loop close to the surface. The entwined mountain became the almost complete circulating mountain of Gundelfingen.

After a further 1.7 km of the river, a half-destroyed Umlaufberg follows, on which Derneck Castle is today. Before the Burgberg constricted, the Lauter flowed in a high loop past Berg Käpfle and the hamlet "Weiler".

Before Unterwilzingen, the Lautertal crosses the Lautertal Fault . This fault extends from Baach (on the Zwiefalter Aach) in the southwest via Oberwilzingen-Erbstetten-Granheim to Frankenhofen in the northeast. The southern clod rejected the displacement, which can also be clearly traced morphologically. The part of the fault south of the Lautertal near Oberwilzingen (see photo) has formed a steep step in the mass limestone with a displacement of approx. 100–115 m. This can even be seen with the naked eye. Prinz (1959) p. 77, analyzed this disturbance and divided it into two partial disturbances and three phases of movement that occurred in different geological ages. For the part south of the Lautertal, the third movement phase, a Middle Miocene - Upper Miocene post-movement has been proven. The disturbance should not have affected the gradient of the Lauter.

Visible large fault , post-movement in the Middle / Upper Miocene, approx. 100 m, near Oberwilzingen , Große Lauter
Fault on the Lower Great Lauter, digital elevation relief. Two extensive limestone bars (hatching) are marked

Another Miocene fault, but probably significantly younger than the Lautertal fault, is a fault near Reichenstein with a jump amount of only 5 - 10 m. This fault is characterized by the fact that it influenced the valley direction of the Große Lauter towards the east.

Recent sediments above the lowest rock bed, especially tufa

The bedrock of the deepened Great Lauter has been filled up again from the recent Pleistocene by various deposits, although the water supply has become low due to the reduction of the catchment areas, the mature karstification and increasing average temperatures. The deposits since the most recent Pleistocene, which are still present today, include limestone pebbles, frost debris / hillside debris, coarse gravel. More or less Holocene age are clayey silty material, more or less organic matter, stony loam, peat, tufa, solid and sand-shaped.

Hoher Gießel, approx. 4 m high gradient in the gorge-like Lautertal to Anhausen
Freshly precipitated limestone tuff : initially a soft, but soon dried out, hard mass
Example of tufa limestone sediment with inclusions
stepped waterfall, demolition of a tufa bar near the Laufenmühle

A typical appearance of the mature karstification in limestone are tufa deposits. In particular, after only slightly high steps and small waterfalls, such as the "Hohen Gießel", more a consequence of cascades that influence the gradient, chemical precipitation of calcium carbonate (CaCO 3 ) occurs, which can be dissolved in karst water up to the chemically possible degree of saturation . Dissolved calcium carbonate is a "normal" component of the karst water of the Swabian Alb. The precipitation process occurred in the interglacial of the Young Pleistocene and then again in the warm Atlantic in large quantities and currently on a smaller scale in most of the streams and rivers of the Swabian and Franconian Jura . In particular when turbulence or pressure relief is pending, e.g. B. after cave or source exits, there is a chemical reaction. Then the gas component CO 2 of the dissolved calcium carbonate can escape and what remains is an initially soft, mostly yellowish sediment mass.

Close to the level of the Hoher Gießel waterfall, there is one of the few karst springs in the Great Lautertal, the blue fountain. The tufa sediment settles and hardens. All small foreign bodies, small animals, leaves, twigs, sand and clay are included. Cavities and overhangs can also arise.

The most important tufa deposits are exposed by a quarry that has only been closed for a few years (near the Laufenmühle). A hardened tufa layer approx. 30 m high and 60 m wide was mined here commercially. In the past, stone blocks that were ideal for local house building were often sawn from the tufa.

See also

Commons artwork

Commons : Images for the Große Lauter  - collection of images, videos and audio files

literature

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  • Enkelman etal (2015), Enkelmann, R, Ruoff, D., Wohnhas, W., In the heart of the Alb; Nature and culture in the biosphere area. Tübingen 2015
  • Ufrecht etal (2016), Ufrecht, W., Bohnert, J., Jantschke, H., A conceptual model of karstification history for the catchment area of ​​the Blautopf (central Swabian Alb), Laichinger Höhlenfreund, 2016

Web links

Individual evidence

  1. ↑ Dongus (1977)
  2. ↑ Carpenter (1965)
  3. ↑ Schreiner 1965, plate 22. Strasser & Sontheimer (2005), p. 86.
  4. ^ Sach & Heizmann (2001)
  5. ↑ "Grimmelfinger layers, Suevicus layers and Kirchberger layers", Sach & Heizmann (2001)
  6. ↑ "The burial masses were removed again in the younger Upper Miocene and the oldest Pliocene." Dongus (2000)
  7. ↑ Strasser (2005) p. 87
  8. ↑ Prinz (1959) p. 59
  9. ↑ Juranagelfluh occurrences in this area are shown in the geological online map 1:50 000 State Office for Geology, Raw Materials and Mining (LGRB).
  10. ↑ G. Wagner (1963)
  11. ↑ Evidence for the tipping: today the still perceptible “cliff line” of the coast of the last Molasse Sea (Lower Miocene) runs between 900 m in the west and 500 m in the east of the Swabian Alb
  12. ^ Villinger (1986), Kiderlen (1931)
  13. ↑ Eberle et al (2007) p. 61
  14. ↑ Dongus (2000)
  15. ↑ Graphics in Dongus (1970), Fig. 1, attached to the map
  16. ↑ See the mapping and inspection of Tillmanns (1984)
  17. ↑ G. Wagner (1961) p. 94
  18. ^ Villinger (1986)
  19. ↑ Dongus (1977)
  20. ↑ Eberle et al (2007)
  21. ↑ Dongus (1977)
  22. ↑ Wagner and Dongus make different statements. Wagner (1938); Dongus (1977)
  23. ↑ Abel (2003)
  24. ↑ LGRB (1974) pp. 124,127
  25. ↑ Bartz (1961); Geyer & Gwinner (2011)
  26. ↑ Dongus (1977)
  27. ↑ Dongus (1977) pp. 355f lists a number of them
  28. ↑ Abel (2003) pp. 19, 88
  29. ↑ quoted from Abel (2003) p. 152
  30. ↑ Important evidence for this is provided by the thorough, multiple researches and considerations on the sedimentation and erosion events that were found in the former water cave Karls- und Bärenhöhle , western Middle Alb. Abel et al (2006)
  31. ↑ Dongus (1977)
  32. ↑ Abel (2003)
  33. ↑ Dongus (1977)
  34. ↑ Hölder (1951)
  35. ↑ Prinz does not provide any information on whether the ineffectiveness is more than a description of the present.
  36. ↑ Prince (1959)
  37. ↑ "The described occurrences of the Laufenmühle (...) belong to the Altholocene according to their fauna", Prinz (1959)