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55-553: The Hürtgen Forest lies at the northern edge of the Eifel mountains and High Fens – Eifel Nature Park ; its terrain is characterized by plunging valleys that carve through broad plateaus. Unlike many areas of Germany in which the valleys are farmed and hilltops are wooded, the Hürtgen Forest's deep valleys are thickly wooded and the hilltop plateaus have been cleared for agriculture. The forest's rough terrain starkly contrasts with that of

110-662: A SW-NE direction far beyond the Rhine valley. Since that folding, the Eifel has largely remained part of the mainland. During the Permian , after the end of the uplifting, the Variscan mountains were heavily eroded, leaving only a relatively flat, truncated upland. For a short time, and only partially, this was later flooded by the sea. Depositions from the Triassic and Jurassic periods have survived in

165-456: A chain from northwest to southeast. The youngest maars are only slightly older than 11,000  years. In the eastern Eifel, volcanism began about 500,000 years ago in the area of today's Laacher See; it extended to the Neuwied Basin to the south, and crossed the Rhine to the east. The quantity of basalt lavas, pumice tuffs and ash tuffs produced by the volcanoes was far greater here than in

220-486: A distinctly stimulating climate; the high elevations being considered as highly stimulating. The Eifel is a clean air area with very low air-chemical pollution. On hot sunny days, there is sometimes an increased concentration of ground-level ozone. Here are a couple of weather station examples for settlements in the Eifel. At the time of the Roman Empire the whole mountain range between the rivers Rhine, Meuse and Moselle

275-439: A plain grading to a base level only at a grand-scale. At the grand-scale peneplains are characterized by appearing to be sculpted in rock with disregard of rock structure and lithology , but in detail, their shape is structurally controlled, for example, drainage divides in peneplain can follow more resistant rock. In the view of Davis large streams do became insensitive to lithology and structure, which they were not during

330-651: A process in nature, is not without controversy, due to a lack of contemporary examples and uncertainty in identifying relic examples. By some definitions, peneplains grade down to a base level represented by sea level , yet in other definitions such a condition is ignored. Geomorphologist Karna Lidmar-Bergström and co-workers consider the base level criterion crucial and above the precise mechanism of formation of peneplains, including this way some pediplains among peneplains. While peneplains are usually assumed to form near sea level it has also been posited that peneplains can form at height if extensive sedimentation raises

385-490: A region is known as a primary peneplain. An example of a primary peneplain is the Sub-Cambrian peneplain in southern Sweden. The peneplain concept is often juxtaposed to that of pediplain . However authors like Karna Lidmar-Bergström classify pediplains as a type of peneplain. On the contrary Lester Charles King held them as incompatible landforms arguing that peneplains do not exist. King wrote: According to King

440-661: A surprise counter offensive in the Ardennes on 16 December 1944, the Battle of the Bulge . The forest was further devastated by fires in the summer of 1945, ignited as the weather warmed leftover white phosphorus munitions . The battle is commemorated in the 1944 Hürtgen Forest Museum , opened in 1983. There are three German war cemeteries; the one at Hürtgen was opened in 1952 and is the resting place of some one hundred postwar victims of mines and unexploded ordnance. Beside other small memorials,

495-419: Is an average of 70 days of full snow cover because the frequency of snow at higher elevations is relatively high (for comparison: Bitburg 35  days, Maifeld 30  days), but the level of snowfall varies from year to year. Snow heights vary on average between 15 cm and 60 cm. The humid Atlantic climate can cause extreme variations though: on 2 March 1987 there was 227 centimetres of snow in

550-432: Is irrelevant and that the term peneplain has been used and can be used in a purely descriptive manner. Further, alternation of processes with varying climate, relative sea level and biota make old surfaces unlikely to be of a single origin. Peneplains that are detached from their base level are identified by either hosting an accumulation of sediments that buries it or by being in an uplifted position. Burial preserves

605-525: Is now regarded as the standard work on the geology of the Eifel. The Eifel and its western continuation into Belgium, the Ardennes , are the remains of a Variscan truncated upland , much of it 400 million years old, that is part of the Rhenish Massif ( Rheinisches Schiefergebirge ). In the area of the Stavelot-Venn Saddle ( Hohes Venn ) are the oldest layers of rock, which originate from

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660-655: Is west/southwest. A relatively dry and milder climate prevails in the wind and rain shadow of the High Eifel. Cold air from Siberia in the higher elevations of the Eifel has less of an impact on weather conditions, as the proximity of the Atlantic Ocean to the Eifel brings milder sea air to the Eifel even in winter. Looking at the long-term averages, even the Snow Eifel only has snow cover for nine consecutive days in winter, as there are no longer lasting cold spells. However, there

715-604: The Cambrian and are around 550 million years old. The Eifel is one of the few volcanically active areas of Germany, as is evinced by numerous discharges of carbonic acid , for example into the Laacher See . The last eruptions, which gave rise to the most recent maars , occurred about 11,000  years ago. The basement in the Eifel, as in the other regions of the Rhenish Massif , consists mainly of Devonian slates , sandstones and limestones , laid down in an ocean south of

770-782: The German Wildlife Route and the South Eifel Holiday Route. Due to its moist and mild Atlantic climate, the Eifel is bisected by numerous streams and small rivers. Impoundment of these streams, especially in the North Eifel has led to the creation of very large reservoir , such as the Rursee , which is the second largest in Germany by volume, and the Urftsee . A feature of the Eifel are its natural lakes of volcanic origin. The largest,

825-621: The Handbook of the Natural Region Divisions of Germany , divided into three major unit (i.e. two-digit) groups and these were subdivided into (three-digit) major natural units. These divisions were subsequently refined in the individual map sheets Trier/Mettendorf , Cochem (both 1974) and Cologne/Aachen (1978) as follows; for the most detailed natural region divisions in Rhineland-Palatinate, fact files were produced by

880-598: The Laacher See , is a collapsed, water-filled caldera , whilst the many maars are water-filled volcanic eruption bowls. The largest maar lake is the Pulvermaar . The Meerfelder Maar has an even bigger basin, but three-quarters of it has silted up. The many rivers and streams of the Eifel drain into the North Sea via the great rivers outside of the Eifel: the Rhine (and its tributary,

935-566: The Moselle ) and the Meuse (with its tributaries, the Rur and Ourthe ). The rivers and streams within the mountain range, together with their larger tributaries, are as follows: Rhine tributaries: Meuse tributaries: Reservoirs Volcanic lakes Despite the interesting geology of the Eifel region, only three comprehensive geological accounts have been produced. In 1822, Johann Steiniger published

990-586: The Old Red Continent and folded and overthrust in the Variscan orogeny. Only on the northern edge of the Eifel, in the High Fens and its environs, do older rocks from the Cambrian and Ordovician outcrop. Rocks of the Carboniferous do not occur in the Eifel itself, but lie along its northern boundary in the region of Aachen . The Devonian rocks were deposited in an oceanic basin , in which erosion debris

1045-714: The Schwarzer Mann in the Schnee-Eifel , stand out from a long way off as long, forested ridges or clearly isolated mountaintops. The highest mountain in the whole Eifel is the Hohe Acht at 746.9 m. It is the only Eifel summit above 700 m. However, many peaks, mountain ridges and large regions, such as the Zitterwald reach heights of over 600 m. These include two dozen peaks with good all-round views, of which many have an observation tower . From north to south they are:

1100-451: The diphthong and the syllable , -fel . The resulting root form Anfil or Anfali would then mean an "area that is not so level". An - would then be a prefix and -fali , which is related to the Slavic polje ("field"), means "plain" or "heath". W. Kaspers (1938) deduces from the surviving form in pago aquilinse the root form aku-ella, akwella and points to its development into

1155-506: The Earth's surface from the upper regions of the Earth's mantle or, in the majority of cases, gathers in a magma chamber, several tens of kilometres deep, at the base of the Earth's crust , from which magma rises at irregular intervals and causes volcanic eruptions. Volcanism in the Eifel is thought to be partly caused by the Eifel hotspot , a place where hot material from deep in the mantle rises to

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1210-477: The Eifel on the Weißer Stein . The mean temperature in the coldest month (January) is -1.5 °C at high elevations, +1.5 to 2 °C in the mountain foreland. There is an average of 110 days of frost, with temperatures below 0 °C in the highlands and an average of 30 to 40 'ice days' when temperatures do not rise above 0 °C. The warmest month (July) only has an average temperature of 14 °C in

1265-564: The High Eifel came to an end about 15 to 20 million years ago, at the same time as that of the Siebengebirge. Volcanism in the western and eastern Eifel is, in contrast to that of the High Eifel, much more recent than that of the Siebengebirge and Westerwald. It began in the West Eifel region of Daun, Hillesheim and Gerolstein about 700,000 years ago and created a chain of ash volcanoes, cinder cones , maars and craters running in

1320-903: The Michelsberg, Häuschen and Teufelsley in the north; the Adert, Hohe Acht and Raßberg in the northeast; the Hochkel, Nerotherkopf, Dietzenley and ruins of the Kasselburg in the central area; the Prümer Kalvarienberg, Hartkopf and Prümer Kopf in the east, the Steineberg and Mäuseberg near Daun, the Hochsimmer and Scheidkopf near Mayen; the Eickelslay and Absberg in the southeast; and the Krautscheid and Hohe Kuppe in

1375-402: The adjoining Rhine Valley . The forest's few roads are winding, narrow, and challenging to navigate. During World War II the rugged terrain of this area was the scene of the long, bloody, drawn-out Battle of Hürtgen Forest , which took place over three months during a cold fall from 19 September 1944 to 16 December 1944. The Germans successfully defended the area while gaining time to launch

1430-679: The area around Hillesheim and Oberbettingen . In the Upper Cretaceous and during the Tertiary , the Eifel was inundated mainly from the north. Remains of Cretaceous rocks were discovered on the High Fens. Scattered patches of Oligocene deposits can be found there and in the Western Eifel. From the Pliocene onwards, the Rhenish Massif, including the Eifel, experienced an uplift. This led to

1485-474: The basis of a significant mining activity for the extraction of building materials since Roman times. Some of the hills are volcanic vents. The peculiar circle-shaped lakes ( maars ) of the volcanic regions formed in volcanic craters. The first volcanic eruptions took place in the early Tertiary centred in the High Eifel and even before the volcanic activity of the Siebengebirge and Westerwald . Volcanism in

1540-559: The cities of Aachen to the north, Trier to the south and Koblenz to the east. It descends in the northeast along a line from Aachen via Düren to Bonn into the Lower Rhine Bay . In the east and south it is bounded by the valleys of the Rhine and the Moselle . To the west it transitions in Belgium and Luxembourg into the geologically related Ardennes and the Luxembourg Ösling . In

1595-417: The coalesced pediments of the pediplains form a series of very gentle concave slopes, a difference with Davis' understanding of peneplains may lie in the fact that his idealized peneplains had very gentle convex slopes instead. However, Davis' views on the subject are not fully clear. Contrary to this view Rhodes Fairbridge and Charles Finkl argue that the precise mechanism of formation (pediplanation, etc.)

1650-454: The difference between pediplains and Davis’ peneplains is in the history and processes behind their formation, and less so in the final shape. A difference in form that may be present is that of residual hills, which in Davis’ peneplains are to have gentle slopes, while in pediplains they ought to have the same steepness as the slopes in the early stages of erosion leading to pediplanation. Given that

1705-652: The edge of the Eifel and formed larger valleys. The Eifel covers an area of 5,300 km and is geographically divided into the North and South Eifel. It is further divided into several natural regional landscapes, some with further subdivisions. Since 2004, part of the North Eifel has been designated as the Eifel National Park . There are also four nature parks in the Eifel (from north to south): Rhineland , High Fens-Eifel , Volcanic Eifel , and South Eifel , although

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1760-461: The first extends only partly into the northern foothills of the Eifel. There are several distinct chains within the Eifel. Since 2004, about 110 km of the Eifel within the German state of North Rhine-Westphalia have been protected as the Eifel National Park nature reserve . Up to 1960, the German part of the Eifel, which belonged to the natural region of the Rhenish Massif , was, according to

1815-540: The first geological map of the area and, in 1853, the Geognostische Beschreibung der Eifel . In 1915 Otto Follmann published a new account, adding to the extent of scientific understanding at that time, the Abriss der Geologie der Eifel ("Abstract of the geology of the Eifel region". In 1986, Wilhelm Meyer finally published the volume, Geologie der Eifel ("Geology of the Eifel"), whose fourth, revised, edition

1870-822: The following classification scheme for peneplains: Rhodes Fairbridge and Charles Finkl argue that peneplains are often of mixed origin (polygenetic), as they may have been shaped by etchplanation during periods of humid climate and pediplanation during periods of arid and semi-arid climate. The long time spans under which some peneplains evolve ensures varied climatic influences . The same authors do also list marine abrasion and glacial erosion among processes that can contribute in shaping peneplains. In addition, epigene peneplains can be distinguished from exhumed peneplains. Epigene peneplains are those that have never been buried or covered by sedimentary rock. Exhumed peneplains are those that are re-exposed after having been buried in sediments. The oldest identifiable peneplain in

1925-548: The higher areas. The level of precipitation decreases significantly from west to east as a result of the rain shadow of the highlands. So the Schneifel receives an average of 1,200 mm of precipitation ( High Fens : 1,400 mm to 1,500 mm), while in Maifeld the average rainfall is only 600 mm. The bioclimatic conditions in the Eifel are favourable. Heat stress and air humidity are rarely present in summer. The Eifel has

1980-452: The local base level sufficiently or if river networks are continuously obstructed by tectonic deformation . The peneplains of the Pyrenees and Tibetan Plateau may exemplify these two cases respectively. A common misconception about peneplains is that they ought to be so plain they are featureless. In fact, some peneplains may be hilly as they reflect irregular deep weathering , forming

2035-459: The name "Eifel" in the following sequence: aquila  > agfla  > aifla  > eifla  > Eifel . Akuella derives from the pre-German and means "land with summits" or "land with peaks". Peneplain In geomorphology and geology , a peneplain is a low-relief plain formed by protracted erosion . This is the definition in the broadest of terms, albeit with frequency

2090-618: The north it is limited by the Jülich-Zülpicher Börde . Within Germany it lies within the states of Rhineland-Palatinate and North Rhine-Westphalia; in the Benelux the area of Eupen , St. Vith and Luxembourg. Its highest point is the volcanic cone of the Hohe Acht (746.9 m). Originally the Carolingian Eifelgau only covered the smaller region roughly around the sources of the rivers Ahr , Kyll , Urft and Erft . Its name

2145-660: The northern and northwestern foothills of the present Eifel in the eastern half of the Arduenna silva of the Romans. West of the Eifelgau lay the Ardennengau , whose name was derived from Arduenna silva . Following the end of the Frankish Empire the name of the old gaue continued to be used in popular language. Over the centuries an ever-larger region was referred to as the Eifel. Today

2200-402: The peneplain. Any exposed peneplain detached from its baselevel can be considered a paleosurface or paleoplain . Uplift of a peneplain commonly results in renewed erosion. As Davis put it in 1885: Uplifted peneplains can be preserved as fossil landforms in conditions of extreme aridity or under non-eroding cold-based glacier ice. Erosion of peneplains by glaciers in shield regions

2255-518: The road that rises from the Kall River Valley to the town of Schmidt incorporated the track of a destroyed Sherman tank . Eifel The Eifel ( German: [ˈaɪfl̩] ; Luxembourgish : Äifel , pronounced [ˈæːɪfəl] ) is a low mountain range in western Germany , eastern Belgium and northern Luxembourg . It occupies parts of southwestern North Rhine-Westphalia , northwestern Rhineland-Palatinate and

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2310-638: The so-called Eifel North-South Zone. This is a region of subsidence , which runs from the Trier Bay in the south to the Lower Rhine Bay in the north. Through this zone existed at one time a sea link between north and south Central Europe. The remains of the sediments laid down at this time have survived to a greater extent in the Maubach- Mechernich Triassic Triangle in the north and in the Oberbettingen Triassic Graben in

2365-568: The southern area of the German-speaking Community of Belgium . The Eifel is part of the Rhenish Massif ; within its northern portions lies the Eifel National Park . The Eifelian stage in geological history is named after the region because rocks of that period reach the surface in the Eifel at the Wetteldorf Richtschnitt outcrop. The inhabitants of the Eifel are known as Eiflers or Eifelers . The Eifel lies between

2420-600: The southwest. The mountains and hills of the Eifel include the following (in order of height in metres above sea level ): (near Schwarzer Mann ) For a list of these and other Eifel mountains and hills see the List of mountains and hills of the Eifel . Many of these prominent points are linked by the Eifel-Ardennes Green Route , which crosses the east and south of the region, the German Volcano Route ,

2475-421: The state information system of the conservation administration (LANDIS): The BfN groups the 3 (two-digit) major unit groups under the combined group designated D45 . Apart from its valleys, the Eifel is a gently rolling plateau from which elongated mountain ridges and individual mountains rise. The majority of these summits do not attain a great height above the surrounding terrain. Several, however, like

2530-563: The streams and rivers cutting into the gently rolling landscape resulting in the present appearance of the low mountain range with its flat plateaus and deeply incised valleys. Due to numerous recent research projects, climate changes since the last ice age can be traced in detail in the Eifel region. Volcanic activity in the Eifel began 50 millions of years ago and continues into the geological present. It created numerous volcanic structures, lava flows and extensive layers of volcanic ejecta made of tuff and pumice , which have formed

2585-542: The surface, and partly by melt-ascent at deep fractures in the Earth's crust. Research has shown that the volcanism is still active; the Eifel region is rising by 1–2 mm per year and there are escaping gases, for example, carbon dioxide (CO 2 ) in the Laacher See . The Eifel is in the Atlantic climate zone with its relatively high precipitation; winters that are moderately cold and long with periods of snow; and summers that are often humid and cool. The prevailing wind

2640-461: The usage of peneplain is meant to imply the representation of a near-final (or penultimate) stage of fluvial erosion during times of extended tectonic stability. Peneplains are sometimes associated with the cycle of erosion theory of William Morris Davis , but Davis and other workers have also used the term in a purely descriptive manner without any theory or particular genesis attached. The existence of some peneplains, and peneplanation as

2695-442: The valley phase of erosion cycle. This may explain the existence of superimposed streams . There are various terms for landforms that are either alternatives to classical peneplains, a sub-set of peneplains or partially overlap with the term. The last is the case of planation surfaces that may be peneplains or not, while some peneplains are not planation surfaces. In their 2013 work Green, Lidmar-Bergström and co-workers provide

2750-401: The western Eifel. East Eifel volcanism came to an end with a huge eruption, as a result of which the magma chamber emptied and collapsed, creating a caldera . Today's Laacher See formed in the caldera. The ashes from the eruption can be detected today in deposits all over Central Europe and as far as Bornholm as a thin layer. Volcanism is caused by magma , which either rises directly to

2805-596: The western part of the plateau. In the eastern part, in the High Eifel and Volcanic Eifel , individual cinder cones and basalt kuppen , like the Hohe Acht and the Ernstberg , emerged as a result of volcanicity in the Tertiary and Quaternary periods and rise above the undulating countryside. The rivers draining into the Moselle , Rhine and Meuse , such as the Our , Kyll , Ahr , Brohlbach and Rur , have cut deep into

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2860-608: The whole German-speaking part of the range between the Rhine, Meuse and Moselle is called the Eifel (including several areas outside of Germany, see the →  Belgian Eifel ), while the French-speaking part in Belgium and France is called the Ardennes . 762 Eifflensis pagus , 772 Eiffelnsis pagus , 804 in pago aquilinse , 838 Eifla , 845 Eiflensis pagus , 855 Eiflinsis pagus , 860–886 Agflinse , 975 Aiflensis pagus , 1051 Eiffila , 1105 Eifla , 1121 Eifla Müller/Schnetz (1937) believe that an -n- has dropped out between

2915-444: Was called Arduenna silva ("high forest"). The oldest record of the name "Eifel" does not occur until the Early Middle Ages . Following the collapse of the West Roman Empire , the Frankish Empire emerged in the territories of present-day France and western Germany. This was divided into gaue (Lat.: pagi ). One of them, the Eifelgau , covered the source regions of the rivers Erft , Urft , Kyll and Ahr , i.e. predominantly

2970-420: Was more recently transferred to the entire region. The Eifel belongs to that part of the Rhenish Massif whose rolling plateau is categorised as peneplain highland ( Rumpfhochland ), which was formed by the erosion of the ancient mountains of the Variscan mountain building phase and subsequent further uplifting. Individual mountain chains, up to 700 m, such as the Schneifel and High Fens , run through

3025-560: Was washed in from the north from the great north continent of Euramerica ( Laurussia or the Old Red Continent ) which was formed by Caledonian mountain building during the Silurian . From the end of the Lower Carboniferous the sea basin was caught up in the Variscan mountain building process, pushed together and uplifted, and thus formed part of the Variscan mountain system that, in the Upper Carboniferous and early Permian , covered large areas of Europe. The Eifel geological structures like main folds and overthrusts can be traced in

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