Field Trip A (23 September 2018): geology and geomorphology of Giessen and its surrounding areas

Rocks of the present-day Rhenish Massif (RM) were formed from Silurian times up to the upper Carboniferous/early Permian, in close connection with the Variscan orogeny. Plate tectonic processes related to this major orogenic event included opening and closing of oceanic basins, terrane accretion, volcanism, sedimentation, orogenic folding and metamorphism as well as nappe formation. Major players included the Old Red Continent in the north, the Avalonia terrane, the Rhenohercynian and Rheic oceans and Gondwana further south (Fig. 3).

Figure 3Plate tectonic reconstruction for the Late Devonian to early Carboniferous (Eckelmann et al., 2014). Red star: position of the autochthonous Rhenish Massif. Blue star: source area of the nappe units in the southeast of the Rhenish Massif.

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These processes led to a large number of sedimentary, magmatic and metamorphic rocks, each representing their depositional, facies and/or geodynamic characteristics and thus providing valuable information for the reconstruction of these geological processes in space and time. Not surprisingly, (para-)autochthonous and allochthonous units are found in close contact with each other. In addition to varying degrees of alteration and post-orogenic displacements, this may well explain the difficulties in reconstructing the Paleozoic geodynamic processes as well as some of the fierce discussions in the recent scientific literature (Eckelmann et al., 2014; Dörr and Zulauf, 2012; Franke, 2012) and references therein). At the end of the Variscan orogenic processes, the RM suffered massive erosion of elevated regions and coeval filling of basin structures, resulting in a widespread peneplain during Permian times.

During the Mesozoic, most parts of the RM were situated above sea level and acted as source regions for clastic sediments in adjacent basins. It is worth mentioning that the region of the RM west of Giessen lacks Mesozoic cover.

Intensive chemical weathering during early Tertiary times is documented by thick clay-rich saprolite layers, locally capped/covered by intraplate volcanics (Eifel, Siebengebirge, Westerwald). These kaolinite-rich soils and saprolites, with locally preserved thicknesses of more than 150 m, reflect the humid tropical climate conditions during their time of formation. Climate conditions subsequently changed towards semi-arid characteristics, resulting in areal denudation of unprotected land surfaces.

During the Quaternary, the RM was severely affected by periglacial processes as well as intense uplift (Fig. 4), with an accumulated maximum uplift of more than 250 m during the last 800 000 years in the uplift center (Eifel area). These led to the present-day morphologic characteristics of the RM, i.e., a large uplifted block with plateau-like regions, maximum heights of around 900 m and deeply incised river valleys (e.g., Middle Rhine, lower Mosel and lower Lahn rivers).

Figure 4Sketch map showing the uplift of the Rhenish Massif during the last 800 000 years (from Meyer and Stets, 2002). Small dots: observation points along rivers. Dashed line: the outer rim of the Rhenish Massif.

Figure 5Simplified geological profile of the Giessen area (modified from Weyl and Stibane, 1980, composite from Gleiberg to Lahn valley and Giessen-Bergwerkswald northwest–southeast, and from Bergwerkswald to Schiffenberg west–east). The main petrographic units are shown: Paleozoic rocks of the Rhenish Massif (blue and gray), Cenozoic sedimentary filling of the north–south-trending subsidence (green and yellow) segments and Tertiary volcanics at the western border of the Vogelsberg volcanic field (purple).

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Thus, morphologic processes during the Cenozoic are dominated by the following:

1. a phase of intense weathering and denudation during humid tropical and semi-arid climate conditions with peneplain formation

2. a phase of pronounced uplift and linear erosion during the Quaternary.

The old castle of Gleiberg (12th century) was built on a small hill (308 m a.s.l. and 70–80 m above the surrounding area). The hill is made up of Miocene columnar basaltic rocks that penetrate graywacke of lower Carboniferous age that are part of the Giessen nappe (Fig. 5).

Depending on weather conditions, this location and especially the castle keep offers a nice outlook and a panoramic view.

Towards the southeast, we look into the small depression of the Giessener Becken, with the foothills of the Vogelsberg in the distance.

To the east, we see the valley of the Lahn river, the corresponding main terrace and a prominent basalt hill (Lollarer Kopf). In the far distance, though morphologically not very prominent, the forested slopes of the main Vogelsberg can be seen.

To the northeast, the Miocene basalt hill of Amöneburg and the Lahnberge of Marburg (early Mesozoic sandstone ridge) are visible.

To the north, behind the village of Krofdorf, there is a large forest area on comparatively infertile graywacke.

To the west, the plateau of Königsberg-Hohensolms, consisting of lower Carboniferous basaltic rocks that are locally known as “Diabas”, can be seen.

To the northwest, a short distance from the prominent Dünsberg (498 m a.s.l.) is visible, a monadnock dominated by allochthonous lower Carboniferous lydite. In the foreground, Vetzberg and Köppel (Fig. 6), both volcanic edifices similar to Gleiberg (Weyl and Stibane, 1980) can be seen. It is worth noting that Gleiberg, Köppel and Vetzberg are aligned along a north–west-running fault line. Based on detailed geochemical and radiometric age studies by Turk et al. (1984), the location of Gleiberg, together with nearby Vetzberg and the small edifice of Köppel, comprise the westernmost eruption centers of the Vogelsberg volcanic field (VB). Columnar jointing is well developed at Vetzberg castle (Fig. 7).

Figure 6Typical landscape west of Giessen with Vetzberg (left) and Dünsberg (right). Own picture, 24 February 2018.

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Figure 7Miocene basaltic rocks with well-developed columnar jointing at Vetzberg castle. Own picture, 24 February 2018.

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Along the road from Gleiberg to Breitscheid (Stop 2), paleozoic rocks (dominantly graywacke, slate, diabase, limestone and also lydite) are exposed in numerous small quarries and roadside outcrops. Occasionally, a transformation of the silicate rocks into clay minerals is clearly visible. The formation of these clay minerals (kaolinite, illite) is attributed to intense chemical weathering during lower Tertiary and Miocene times (Felix-Henningsen, 1994). In adjacent areas of the Westerwald volcanic field, these clay-rich lithologies were covered by upper Tertiary volcanic rocks, resulting in an effective protection blanket against further weathering and especially erosion. Therefore, these clay deposits were to become the primary commodity for the famous ceramic industry in the Westerwald area, known as the “Kannenbäckerland”.

The quarry is located about 1 km south of the village of Philippstein. Exposed rocks are mafic volcanics of Givetium/Adorfium age (Middle to Early Upper Devonian; Deutsche Stratigraphische Gesellschaft, 2016) as well as red iron ore deposits (Fig. 11). At the eastern wall of the quarry, several galleries of the abandoned mine “Maria” have been cut off by quarry activities. All rock units were deformed during the Variscan orogeny.

Figure 10Inside the limestone cave Herbstlabyrinth, Breitscheid (Schauhöhle Herbstlabyrinth Breitscheid 2018, © K. P. Kappest).

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Figure 11Schematic sketch map of a Devonian submarine volcanic edifice in the Lahn-Dill area (from Nesbor, 2007). White rectangle: segment exposed at the Philippstein quarry (Stop 3).

In the lower parts of the quarry, columnar jointing is clearly visible. These flow units were then covered by volcaniclastic lithologies (Nesbor, 2007). On top, the volcanics are present as pillow lavas, tubes and pillow fragments, indicating a submarine environment. Obviously, the lava split up into several lava tubes. Contact with seawater caused glassy rims, with the basaltic melt that is still hot flowing inside. Depending on the eruption rates, these lava tubes may have piled up to impressive volcanic masses.

The reddish iron ores belong to Lahn-Dill-type deposits, e.g., exhalative iron oxide mineralization associated with basaltic volcanic centers during Middle to Upper Devonian times (Von Raumer et al., 2017). In a first step, mobilization of Fe and associated Ca and Si was caused by hydrothermal alteration and leaching of subjacent submarine basaltic volcanics (Flick, 2010). Subsequently, the rising Fe-bearing hot fluids encountered cool oxidizing water, resulting in the precipitation of iron oxides and hydroxides. For a more detailed discussion of ore genesis in the RM, please see Von Raumer et al. (2017).

Iron ore mining in the Lahn-Dill ore district has been documented since the Celtic area, about 2000 years ago. Numerous Fe ore mines were operating during the 19th and 20th century. The last mine (Grube Fortuna north of Solms-Oberbiel) was closed down in 1983.

Several small basins and graben structures connect the morphologic end of the Upper Rhine Graben with the graben structures of northern Germany. These include the Hanau-Seligenstädter Senke, the Wetterau, the Horloff-Graben, the Giessener Becken and the Amöneburger Becken. Thus, unconsolidated sediments of Cenozoic age are widespread in the regions north and south of Giessen (Fig. 2). Pleistocene loess cover is most pronounced in the basin areas, e.g., Amöneburger Becken, Wetterau and Horloff-Graben (see Field Trip B for details).

It should be mentioned that, amongst these small subsidence structures, only the Horloff-Graben is of post-volcanic age. The morphologically well-defined Horloff-Graben incises into the southwestern section of the Vogelsberg, forming a north–south-running graben structure, 20 km long and 5 km wide (Figs. 2, 12). Graben sediments are of Pliocene and Pleistocene age, with several brown coal seams being developed within the Pliocene pile. Despite their very young age, those brown coal seams were extensively exploited underground and later on in open-pit mines. Mining activities ended in 1991. Subsequent flooding of the open pit gave rise to the so-called “Wetterauer Seenplatte”, now widely used for local recreation, water sports and nature protection.

Figure 12Morphological map of the Vogelsberg area, with the characteristic star-shaped drainage pattern. The highest point of the volcanic field (Taufstein) is indicated by the black triangle. The town of Giessen is also shown, as well as the post-volcanic Horloff-Graben and Hungen-Langd (Stop 4).

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Figure 13Abandoned quarry, about 500 m east of Hungen-Langd (Stop 4) (modified from Nesbor, 2014). Composite sketch map of the quarry walls. Western segment: four lava flows (unit I to IV), each between 5 and 8 m thick, with well-developed breccia zones at their basis and upper regions. Intercalated between the lava flows are tuff layers, dominated by mafic ash and fragments of country rock. Central part: pyroclastic unit (unit V), about 4 m thick, cutting the lava flows and dipping ca. 45^∘ towards southeast, dominated by tuff breccia that contains basanitic blocks, up to 1 m in size. Lapilli-size particles of the tuff breccia show very few vesicles. Unit VI: 1 to 4 m of pyroclastics with different properties, overlying unit V, characterized by highly vesicular scoria, embedded in a lapilli and ash matrix. Eastern segment: massive alkali basalts (unit VII), overlying the pyroclastic sequences, with clearly visible platy and columnar jointing.

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VB, located to the east of Giessen, was active during the Miocene. With an area of 2500 km² and a total volume of at least 500 km³, it is considered the largest volcanic field by volume in central Europe (Reischmann and Schraft, 2009; Fig. 12).

Landscape structure of this huge volcanic field comprises four distinct units. The central parts are known as “Oberwald” above 600 m a.s.l. and “Hoher Vogelsberg” between 600 and 500 m (Leßmann et al., 2000). The “Unterer Vogelsberg” forms a zone of up to 20 km wide around the Hoher Vogelsberg. The volcanic layers extending to the northwest are known as the “Vorderer Vogelsberg”. The Taufstein (774 m a.s.l.) and the Hoherodskopf (764 m) close by have the highest elevations.

Several boreholes provide important information on the minimum size and volume of VB volcanic rocks as well as the internal structures of the volcanic masses (Reischmann and Schraft, 2009). It should be emphasized, however, that the borehole “Forschungsbohrung Vogelsberg 1996”, that penetrated the Central Part of the VB (Oberwald), did not reach the pre-volcanic basis, despite a total coring of 656 m of volcanic rocks. Thus the estimated volume of 500 km³ must be regarded as a minimum mass.

Those boreholes, in conjunction with detailed field and radiometric studies, reveal new insights into the genesis of this huge volcanic edifice. Vogelsberg volcanism comprised a main activity phase at 19–16 Ma and, separated by a period of magmatic quiescence, a final phase at around 14 Ma (Nesbor, 2014; Abratis et al., 2015). Volcanism of the main phase started with basanitic to alkali basaltic magmas and pyroclastics, followed by dominantly trachytic rocks. Phreatomagmatic eruptions and maar structures occurred quite frequently (Nesbor, 2014). After a period of magmatic quiescence, volcanic activity recommenced at about 14 Ma with the eruption of alkali basaltic and basanitic lava flows, with eruption centers being essentially confined to the Oberwald region.

During the magmatic rest period, erosive and pedogenic processes dominated, causing leveling of volcanic edifices and a strong pedogenic overprint due to tropical–subtropical and humid climate conditions. These processes gave rise to a widespread erosional surface, which is still visible as a morphological step (Abratis et al., 2015).

Final volcanic activity was essentially concentrated in the central Oberwald region and dominated by low-viscosity mafic lava flows. Although volumetrically subordinate, these younger lava flows covered older volcanic sequences and erosional features. Due to a well-established climate change during the Langhian towards moderate and rather dry conditions, the final lava flows are much better preserved, thus giving the Vogelsberg volcanic field the appearance of a huge basaltic shield volcano (Nesbor, 2014).

The only rocks that are locally preserved are remnants of intense weathering of Vogelsberg volcanic rocks during Burgidalian times, e.g., Fe-rich crests and saprolite, the latter with thicknesses of more than 50 m (Schwarz, 1997) and most likely related to the mid-Miocene Climate Optimum.

Taking into account the field evidence from the Rhenish Massif to the west, we can emphasize two Cenozoic periods of intense chemical weathering, e.g., a lower Tertiary period, documented in widespread kaolinization of Paleozoic rocks, and a mid-Miocene period, which created Fe crests and saprolite on Vogelsberg volcanics that are 19–16 Ma old.

The old quarry is located about 500 m east of Hungen-Langd and provides an excellent view into the internal structure of the Vogelsberg volcanic edifice (Ebhardt et al., 2001; Nesbor, 2014; Reischmann and Schraft, 2009).

In the western segment of the quarry, four lava flows of basanitic to alkali-basaltic composition are exposed, each between 5 and 8 m thick, with well-developed breccia zones at their basis and upper regions (Fig. 13). Intercalated between the lava flows are tuff layers, which are dominated by mafic ash and fragments of country rock (e.g., Buntsandstein). Thus, volcanic activity included both effusive and explosive characteristics.

Figure 14Columnar jointing in former lake lava, eastern segment of the old quarry, Hungen-Langd (Stop 4). Stefan Schorn, © Reinhold, 20 March 2017.

In the eastern part of the quarry, the lava flows were blown away by a younger explosive event which created a crater wall with a dip of ca. 45^∘ towards southeast. Pyroclastic rocks closest to the crater wall are dominated by tuff breccia that contain basanitic blocks, up to 1 m in size. Lapilli-size particles of the tuff breccia show very few vesicles. Thus the crater-forming event is most likely due to the interaction of rising hot mafic magma with groundwater at shallow depth, causing a phreatomagmatic explosion that destroyed the lava flows and created a maar-type conical crater.

The initial maar deposits are overlain by ca. 1 to 4 m of pyroclastics with different properties. This sequence is characterized by highly vesicular scoria, embedded in a lapilli and ash matrix. Obviously there was a change in eruptive behavior towards lava fountains and effective degassing, most probably related to a lack of groundwater supply.

The volcanic rocks that rest on this layer of highly vesicular scoria occupy the entire eastern section of the quarry. They consist of massive alkali basalts with clearly visible platy and columnar jointing due to comparatively slow cooling and shrinking (Fig. 14). This is best explained by further magma supply from below, ongoing degassing and prohibited groundwater influx, resulting in a slowly cooling lava lake that completely filled the conical crater structure.

No data sets were used in this article.

Frank Volker wrote the text and participated in the fieldwork. Stefanie Menges participated in the fieldwork and took the photographs of Figs. 6 and 7.

The authors declare that they have no conflict of interest.