Fig. 3. Schematic cross-section of the Eichsfeld-Altmark High

r – Rotliegend (Lower Permian), Ca1 – Werra Carbonate, A1 – Werra Anhydrite,
Ca2 – Stassfurt Carbonate, A2 – Stassfurt Anhydrite, Na2 – Stassfurt Salt,
T3 – Leine Clay, Ca3 – Leine Carbonate, A3 – Leine Anhydrite

Borchert and Baier (1953) demonstrated that in the Zechstein basin all thick marine sulphate horizons were originally precipitated as Gypsum. Kosmahl (1969) confirmed this for A3 as he found pseudomorphs of swallow-tail crystals which are typical of Gypsum origin. Later, during burial, the Gypsum was converted to anhydrite due to the increased load and thus pressure of the overlying Zechstein and Triassic strata (Langbein, 1987). This conversion process is discussed below. Uplift of central Europe started during the Cretaceous. South and west of the Harz Mts. more than 1000 m of Mesozoic rocks have been eroded, reducing the burden on the anhydrite and consequently the pressure. More over, during the uplift the anhydrite came in to contact with groundwater. As a result of this process, the anhydrite near the surface was rehydrated. The texture of crystals has been more or less completely changed by the regypsification, but macrostructures, such as bedding planes, clay flasers and chicken wire fabrics, are preserved (Reimann, 1991). Gypsum doming and diapirism in A1 is demonstrated by three examples located near Osterode at the western margin of the Harz Mts. (Fig. 4): Schimpf Quarry, Hellenberg Quarry and Rötzel. The thickness of A1 in the Osterode area is about 100–200 m. The detailed mapping of a large area near Nordhausen at the southern margin of the Harz Mts. yielded additional information about the Gypsum doming diapirism (Fig. 2). SCHIMPF QUARRY West of Osterode, there are several Gypsum quarries with a combined length of several kilometres along the escarpment of the Söse River. These quarries allow for a two-dimensional, often also three-dimensional, view of the Upper A1 and its contact with the overlying Ca2 (Fig. 5). The boundary of A1 with Ca2 is wavy. Formerly it was supposed that this wavy surface is the result of recent partial leaching and underground erosion of the Gypsum, or that it was overlooked (cf. Herrmann and Richter-Bernburg, 1955; Herrmann, 1957). Measurements of the dip of Gypsum bedding planes showed that they are parallel to the outline of the domes (Fig. 5). In some cases the entire shape of diapirs can be reconstructed. There are round cupolas with a horizontal top and steep to vertical slopes that be come shallower downwards (Fig. 6). The Upper part (5–10 m thick) of the Gypsum unit is laminated. My observations and the information given by the quarry manager (S. Brandt) indicate that this part of A1 is very pure. Fig. 4. Sketch-map of the Osterode area and occurrence of Gypsum domes and diapirs The abbreviations of stratigraphic units are explained in Figure 3 Ten metres below the diapirs the Gypsum is horizontally bedded, bedding planes show a larger detachment and some sections show flaser structure. There are selenite horizons in the lower part of A1 whereas no selenite has been found within the diapirs (Fig. 7). HELLENBERG QUARRY The relation of the overlying Ca2 to the rising Gypsum masses can best be seen in a disused quarry at Hellenberg, 2 km away from Osterode (Fig. 8) where an elongate ridge consisting of quarried Ca2 rocks is exposed. The underlying A1 is also exposed in some places. Ca2 consists of well-bedded dark grey dolomudstones and dolowackestones; the beds are a few centimetres to half a metre thick. Ca2 is heavily deformed by slumping, sliding, folding and faulting (Figs. 8–11). The main fold axis is marked by the highest position of the underlying Gypsum (Fig. 9). It can be traced throughout the quarry, and strikes about 130° (Fig. 10). Slump directions are perpendicular to this direction. Bedding planes of Ca2 dip at 20–40° at right angles to the fold axis (Figs. 8 and 10). The northern part of the quarry is dominated by folding (Fig. 11A). At the fold axes, dolomite beds are brecciated. Sliding is the prevailing process at the western and southern parts of the quarry. Carbonate blocks have slid downslope. Slickensides are uneven, but always perpendicular to the main axis (Fig. 11B). There is no secondary calcite that would indicate deformation in a solid state at the slickensides. The temporal succession of events can be reconstructed in some cases (Fig. 11B); slickensiding took place after sliding. All this deformation took place in a semi-lithified state of the Ca2 carbonate. At some places slickensides have nearly horizontal striae, indicating that parts of the Ca2 moved away from the rising Gypsum ridge. It seems that thin-bedded dolomudstones are slumped whereas thick beds reacted by folding and sliding with curved slickensides (Fig. 11A). At the south side of the quarry, there are thin layers or lenses of black coarse crystalline dolomite on top of Ca2, apeculiarity in the Zechstein. The crystal size of the dolomite is up to five millimetres. In the Osterode area, these crystals have been found in several exposures always at the top of Ca2. These crystals were called by geologists of the 19th century, on account of their black colour, “Anthrakonit”. This means that the complete Ca2 horizon is exposed in the quarry. Therefore, the total thickness of Ca2 in the quarry can be estimated as less than 10 metres. The normal thickness of Ca2 in the area amounts to 40 m, as in the quarry of Ührde, about two km away from the Hellenberg Quarry; thus more than half of the thickness of Ca2 typical of the area was removed from the ridge by slumping and sliding or was not deposited. RÖTZEL HILL The Rötzel is an elongate ridge south-west of Osterode (Figs. 4 and 12–14). The ridge is about 200 m wide at the base, but only a few metres wide at the top. It is about 30 m high and can be traced morphologically over a distance of two kilometres. Several small disused quarries give insight into the internal structure of the ridge (Fig. 13). The core of this ridge consists of A1 Gypsum which is overlain by Ca2 dolomudstones. At the slope of the ridge, A2 is exposed in places. At the top A1 has pierced its Ca2 roof and is in contact with A2. Near the contact with Gypsum, dolomite occurs as scattered unrounded clasts some millimetres to some centimetres across. In some places Gypsum fills small cavities within this brecciated dolomite (Fig. 14). North of the top there is a second protrusion of A1 that does not reach A2 (Fig. 13). Near the quarry base a small ridge of Gypsum, vertically foliated parallel to the direction of the gypsum anticline, is exposed.

Fig. 5. A1 Gypsum diapirs at Schimpf Quarry (after Paul, 1987) Fig. 6. Map and section of a Gypsum dome at Schimpf Quarry A–B – position of the section; the scale is for horizontal and vertical directions; notice that the left part of the section shows interpreted part located out side map shown in the Upper part of the figure NORDHAUSEN AREA South of the Harz Mts. at Nordhausen (Fig. 2), the cover of Quaternary deposits above the Zechstein is thinner than in the other areas around the Harz Mts. Paul et al. (1998) mapped an area of about 40 km² in the scale of 1:10,000, especially focusing on the sulphate horizons of the Zechstein (Fig. 15). This mapping yielded detailed information about the deformation of the sulphate. It was found that all over the mapped area, A1 was completely folded as in a fold belt. This was neither expected nor observed before, as in non-Alpine Central Europe the post-Variscan strata are a flat-lying layer-cake. Narrow and acuate anticlines are in contrast to broad and gentle synclines. The types of deformation are roughly the same as in the Osterode region. The dip of the beds varies between vertical and horizontal. Axes of individual anticlines and synclines can be traced over distances of several kilometres. Anticlines are about 0.5 to 1.5 km away from each other. Long anticlines prevail in contrast to round cupolas. All the folds strike more or less in the same direction: about 120°. OTHER AREAS OF GYPSUM DOMES AND DIAPIRS At the eastern border of the Rheinisches Schiefergebirge near Adorf, Gypsum of the Werra Anhydrite (A1) has been extracted since late medieval times from an underground pit which is now closed. Due to its location near the palaeocoast-line of the Zechstein sea, a few clay layers are intercalated with the Gypsum; typically, there are three Gypsum beds. The total thickness of A1 is about 40 m (Kulick, 1987). Finkenwirth (1982) described, from the lower most Gypsum bed, round Gypsum domes 10–20 m in diameter and 10 m in height. Slopes of the domes are up to 45° steep. The claybeds covering the Gypsum are also upwarped and deformed. There is no information about the form of the domes and their preferential direction. Schachl (1954) reported, from rock salt mines of the Middle Triassic Muschelkalk in south-west Germany, that the anhydrite at the base of the rock salt forms domes several metres high; normally, the anhydrite is only several metres thick. The thin layer of salt clay between the anhydrite and the rock salt is partly involved in doming, partly missing on top of the high. Outside the Central European Basin, Gypsum diapirs were described from the Triassic in the Betic Cordillera in southern Spain by Calaforra and Pulido-Bosch (1999). INTERPRETATION AND DISCUSSION Gypsum doming and diapirism are quite common features in the Zechstein around the Harz Mts. Former interpretations of these features are quite different: Fulda (1929) explained the A3 cliffs by a primary rise of precipitation due to an increased brine flow in convection cells; Weber (1931) and Richter (1934) thought that the A3 domes were included in the uplift of the rock salt – most workers agreed with this opinion and drew in their diagrams and drafts faults between Gypsum and rock salt (cf. Seidl, 1914; Fleischer, 1960). This interpretation was also adopted in text-books at the time (Lotze, 1938; Borchert, 1959). Richter-Bernburg (1985) described these “cliffs” as problematic structures of partly tectonic origin and partly synsedimentary precipitations. Langbein (1987) cited Hemmann (1972) and concluded that the cliffs “remain especially problematic”. Fig. 7. Bottom-grown selenite crystals (Schimpf Quarry; A1) Width of the photo – 20 cm (photo T. Paul) In contrast to these opinions, Hemmann (1972) realized that Gypsum diapirism is in dependent of salt diapirism. He also noticed that only the Upper parts of A3 were included in the movement of the sulphate. From the high amount of rock salt crystals within the anhydrite domes and the high percent age of Gypsum within the rock salt above the domes, he concluded that the sulphate at the time of uplift was still Gypsum, highly mobile and containing a large volume of water. Although Hemmann (1972) and Schachl (1991) did not use the term diapir – mainly for linguistic reasons, they used the German word “Klippe” meaning “cliff” – it is clear that large anhydrite clasts of up to five metres across occurring within the rock salt adjacent to the domes prove that the surface of the sulphate penetrated the salt roof and parts of the sulphate broke off and slid away from the diapir (Fig. 1). These processes occurred before the Gypsum was converted to anhydrite. Anhydrite is brittle, not ductile, and not mobile like rock salt. The observations of the A1 domes and diapirs below the Ca2 dolomites by Paul (1987) and Williams-Stroud and Paul (1997) enlarged the knowledge of Gypsum diapirism in other Gypsum horizons. In the Hellenberg Quarry, the rise of the underlying Gypsum at the main axis caused slumping, sliding, folding and slickensides of the overlying dolomite (Ca2). Fig. 8. Sketch-map of Hellenberg Quarry, west of Osterode Direction and dip of Staßfurt Carbonate (Ca2) beds; A1 – Werra Anhydrite; the interior of the quarry is covered with rubble; A–B – location of cross-section shown in Figure 9; thick line – position of main axis Fig. 9. Schematic cross-section of the Hellenberg Quarry along the A–B line shown in Figure 8 Thin lines indicate bedding planes; the thick line represents the boundary of dolomite (Ca2) and underlying Gypsum (A1) Fig. 10. Slump structures at the Hellenberg Quarry The drawing-lines are bedding planes of Ca2; drawing after a photo My observations confirm Hemmann’s (1972) description but the interpretation differs in several aspects. Hemmann (1972) thought that Gypsum diapirism is triggered by water liberated due to the conversion of Gypsum to anhydrite. After Borchert and Baier (1953) it was thought that about 0.5 m³ of water is discharged from 1 m³ of Gypsum. The detailed conditions of the conversion are still under discussion (Braitsch, 1962; Hardie, 1967; Langbein, 1968, 1987; Langbein et al., 1982; Warren, 1999). The depth at which conversion takes place depends on temperature, geothermal gradient, lithostatic pressure and the types and concentrations of pore brines. Most likely, these processes took place at a depth of about one hundred metres (Marsal, 1952); for Zechstein, Langbein (1987) assumed that the minimum depth was 100 m. The Upper part of the Gypsum bed which is included in the diapirism movements differs in terms of structure and composition from the lower part. It is assumed that the Upper parts of A1 and A3 had relatively high contents of pore water because the original deposit was Gypsum mud in contrast to the lower part which consisted – at least partly – of bottom-grown Gypsum crystals (cf., e.g., Langbein, 1987; Denison and Peryt, 2009). In both A1 and A3 the anhydrite is very pure and had most likely been precipitated from highly saline waters, and the Upper parts of original Gypsum units were precipitated at higher salinities than their lower parts. The salinity of the pore water influences the conversion of Gypsum to anhydrite (e.g., Langbein, 1987). The mobile parts of A1 and A3 were at the top of the units, and it is characteristic that in all examples only the Upper part of the original Gypsum unit was involved in doming and diapirism. The Gypsum domes and diapirs around the Harz Mts. and else where are relatively small in size in comparison to salt diapirs. It can be assumed that they could get larger and rise higher, if the amount of mobile Gypsum was larger or the overburden was higher. An other factor which might influence the size and height of the domes and diapirs was the bulk of escaping water, pore water and water produced by the conversion of gypsum to anhydrite. ORIENTATION OF GYPSUM RIDGES In the Nordhausen area there occur round cupolas, though elongate ridges or anticlines prevail (Fig. 15). In the Osterode area the A1 diapirs strike between 90 and 120°; in the Nordhausen area they are strictly about 120° (Fig. 15). The A3 diapirs north of the Harz Mts. strike in various directions: Hemmann (1972) reported strikes for the Bernburg mining district being mainly 110–150°, but also 20–50°; in the Stassfurt district they are about 50°; in the Aller River valley about 140 and 50°. It seems that the A3 diapirs strike parallel and normal to the direction of the salt diapirs, but these observations were made on Gypsum diapirs located on the slopes of large salt diapirs, and therefore their orientation may have been changed. Fig. 11. Hellenberg Quarry A – folds in Ca2 at the Hellenberg Quarry (breadth – 2 m); B – horizontal slickensides are younger than sliding structures; length of the rule is 1 m Fig. 12. Simplified cross-section of the Rötzel diapir, now a Nature Reserve A1 – Werra Anhydrite, Ca2 – Stassfurt Carbonate, A2 – Stassfurt Anhydrite Fig. 13. Sketch-drawing of the central part of Figure 12 Red quadrangle shows position of Figure 14 Fig. 14. Rötzel diapir A – vertical contact of white Gypsum (A1) on the left side and brecciated black and grey carbonate (Ca2) at the right side; the boundary between both rocks is jagged; grey spots within the Gypsum consist of dolomite; the dolomite is completely brecciated (length of the rule – 1 m); B – angular carbonate dolomite clasts with out matrix (length of rule – 5 cm); C – Gypsum within the dolomite (Ca2), most likely, the fill of a cavity In the case of A1 in Osterode and Nordhausen areas, the orientation of Gypsum ridges is exactly parallel to the direction of Hercynian faults (like the Northern Harz fault). Most likely, these movements took place during the Cretaceous and later, but it seems that already during the Zechstein times a similar strain and stress field existed that was characteristic for later times. It is possible that small faults or irregularities of the overlying sediments triggered the rise of the Gypsum and controlled the direction of the elongate ridges. AGE OF GYPSUM DIAPIRISM As previously mentioned, Gypsum doming and diapirism began relatively early: in the case of A1, before the overlying carbonates were completely lithified, and in the case of the A3, when the thickness of the overlying rock salt was less than 30 m, as indicated by large anhydrite clasts within the salt bed (Fig. 1). The overlying Stassfurt Carbonate in the Hellenberg Quarry was not yet completely lithified when Gypsum doming took place, but in the Rötzel Quarry, the already hard, lithified dolomite is broken into small angular clasts near the Gypsum diapir. This difference may depend on the nature of carbonates: thin-bedded clay-like dolomudstones are pliable, whereas thick-bedded pure dolowackestones are more brittle. In addition, the processes of lithification and dolomitization are slowed down by thin clay layers. Hemmann (1972) and Schachl (1991) described, from several localities, large anhydrite blocks or clasts near the anhydrite domes within the Leine Salt (Na3). This is an indication of a very early uplift of the Gypsum during the precipitation of the rock salt. Therefore, Gypsum diapirism started very early, before the overburden necessary for the conversion of Gypsum to anhydrite was reached or the depth at which the conversion occurred was smaller than previously assumed. The duration of uplift is not known, but it was terminated by the conversion of Gypsum to anhydrite. In A3, the growth of the diapirs stopped at the so-called “Anhydritmittel” (am1), an alternation of anhydrite and salt layers. It is as sumed that the growth was terminated when equilibrium between the hydrostatic pressure and the pressure of the lithostatic overburden was reached. Fig. 15. Map of Gypsum cupolas, anticlines and synclines in the area north of Nordhausen Zechstein strata are cropping out, mainly Werra Anhydrite and Stassfurt Carbonate, between the Variscan Paleozoic rocks of the Harz Mts. and the Lower Triassic Buntsandstein REASONS FOR GYPSUM UPLIFT The uplift of Gypsum compared to rock salt or carbonates may have had several reasons: a high content of pore water in the sediment led to lower densities of the Gypsum mud than of semi-lithified carbonates or rock salt; compaction and dewatering brought additional amounts of water below impermeable screening rock salt or carbonates (mudstones and wackestones); conversion of Gypsum to anhydrite which started in the lower parts of Gypsum beds brought additional water to the Upper parts. Due to the conversion of Gypsum to anhydrite the volume of both water and anhydrite was increased by about 10% (Langbein, 1987). If the overlying strata hinders or prevents the escape of water, the hydrostatic pressure rises. Finally, Gypsum and water liftup its roof or, if there are joints, penetrate the overlying strata. In any case, the buoyancy was so great that the Gypsum mud ascended at least 50 m. The uplift stopped when the potential was exhausted, or when the Gypsum mud had the same density as the host rock, or if most of the porewater had escaped by im per ect sealing horizons. CONCLUSIONS Gypsum domes and diapirs are known from three Zechstein sulphate units around the Harz Mts. It is a common feature and is independent of salt diapirism. The uplift of the Gypsum started very early before the conversion to anhydrite took place and before the overlying carbonate beds were completely lithified and when the overlying sediments were only several tens of centimetres thick. Only the Upper layers of the Gypsum bed were involved in the movements. These layers reacted like Gypsum mud and had, most likely, an other composition (less carbonate content), structure (lack of selenite horizons) and/or higher content of pore water than the rest. The conversion of Gypsum to anhydrite brought additional water into the system, increased the hydrostatic pressure and favoured the uplift of the gypsum. Until now, the domes and diapirs of Zechstein sulphate horizons have been only observed from areas around the Harz Mts. In this area there are excellent conditions to investigate Zechstein evaporites. For 200 years salt was mined and at the surface there are several quarries of Zechstein sulphates, and the Harz region is the best-investigated area in the Zechstein Basin. There is no reason to assume that Gypsum domes and diapirs are restricted to the Harz Mts.; instead it is highly probable that they occur in many areas of the Zechstein Basin. Acknowledgements. Many thanks are due to M. Brandt, manager of Gypsum quarry Schimpf (VG-Orth GmbH & Co.KG), who during the years made possible frequent excursions and visits to the quarries. Till Paul helped to produce digital drawings and made some photos. The original manuscript was reviewed by Dr. S. Burliga and Professor F. Orti who gave valuable critics, remarks and suggestions for improvement. REFERENCES Behr, E.M., 1960. Geologische Beobachtung am Hauptanhydrit des Staßfurt-Egelner Sattels im Bereich des Kaliwerkes Staßfurt Schacht VI/VII. Freiberger Forschungshefte, C 90: 88–105. Borchert, H., 1959. Ozeane Salzlagerstätten. Bornträger, Berlin. Borchert, H., Baier, E., 1953. Zur Metamorphose ozeaner Gipsablagerungen. Neues Jahrbuch für Mineralogie, Abhandlungen, B 86: 103–154. Braitsch, O., 1962. Entstehung und Stoffbestand der Salzlagerstätten. Springer, Heidelberg. Calaforra, J.M., Pulido-Bosch, A., 1999. Gypsum karst features as evidence of diapiric processes in the Betic Cordillera, Southern Spain. Geomorphology, 29: 251–264. Denison, R.E., Peryt, T.M., 2009. Strontium isotopes in the Zechstein (Upper Permian) anhydrites of Poland: evidence of varied meteoric contributions to marine brines. Geological Quarterly, 53 (2): 159–166. Everding, H., 1907. Zur Geologie der deutschen Zechsteinsalze. In: Festschrift zum X. Allgemeinen Bergmannstag Eisenach (ed. F. Beyschlag): 25–133. Königlich preußisches geologisches Landesamt, Berlin. Finkenwirth, A., 1982. Die Gipslagerstätte der Grube Pöhlen in der Randfazies des Zechstein 1 bei Diemelsee-Adorf/Ostsauerland. Unpublished diploma thesis. University Clausthal. Fleischer, S., 1960. Die stratigraphische, fazielle und tektonische Ausbildung des Hauptanhydrits auf dem Berlepsch-Maybach-Schacht in Staßfurt. Freiberger Forschungshefte, C90: 52–87. Fulda, E., 1929. Über „Anhydrit-Klippen“. Kali, 23: 129–133. Hardie, L.A., 1967. The Gypsum–anhydrite equilibrium at one atmosphere pressure. American Mineralogist, 52: 171–200. Hemmann, M., 1968. Zechsteinzeitliche Gips/Anhydrit Umwandlung, Anhydritklippenbildung und zugehörige Erscheinungen in der subherzynen Leine-Serie. Mineralogie. Deutsche Akademie der Wissenschaften, 10: 454–462. Hemmann, M., 1972. Ausbildung und Genese des Leinesteinsalzes und des Hauptanhydrits (Zechstein 3) im Ostteil des Subherzynen Beckens. Berichte der Deutschen Gesellschaft für geologische Wissenschaften, B16: 307–411. Herrmann, A., 1957. Der Zechstein am südwestlichen Harzrand. Geologisches Jahrbuch, 72: 1–72. Herrmann, A., Richter-Bernburg, G., 1955. Frühdiagenetische Störungen der Schichtung und Lagerung im Werra-Anhydrit (Zechstein 1) am Südwestharz. Zeitschrift der Deutschen Geologischen Gesellschaft, 105: 589–702. Jung, W., Gerlach, R., Knitzschke, G., 1969. Zur Feingliederung des Hauptanhydrits (A3) im zentralen Zechsteinbecken. Geologie, 18: 1164–1172. Kosmahl, W., 1967. Grauer Salzton und Hauptanhydrit des Zechsteins in Nordwestdeutschland. Geologisches Jahrbuch, 84: 367–406. Kosmahl, W., 1969. Zur Stratigraphie, Petrographie, Genese und Sedimentation des gebänderten Anhydrits (Zechstein 2), Grauen Salztones und Hauptanhydrits (Zechstein 3) in Nordwestdeutschland. Geologisches Jahrbuch, Beiheft, 71: 1–129. Kulick, J., 1987. Zechstein am Westrand der Hessischen Senke. In: Zechstein 87 (eds. J. Kulick and J. Paul). Internationales Symposium. Exkursionsführer, 2: 39–80, Wiesbaden. Langbein, R., 1968. Zur Petrologie des Anhydrits. Chemie der Erde, 27: 1–38. Langbein, R., 1987. The Zechstein sulphates: the state of the art. Lecture Notes in Earth Sciences, 10: 143–188. Langbein, R., Peter, H., Schwahn, H-J., 1982. Karbonat- und Sulfatgesteine. VEB Deutscher Verlag Grundstoffindustrie, Leipzig. Lotze, F., 1938. Steinsalz und Kalisalze – Geologie. In: Die wichtigsten Lagerstätten der Nicht-Erze. III, part 1 (ed. O. Stutzer). Bornträger, Berlin. Lotze, F., 1957. Steinsalz und Kalisalz, Gebrüder Borntraeger, Berlin. Marsal, D., 1952. Der Einfluß des Druckes auf das System CaSO4–H2O. Heidelberger Beiträge zur Mineralogie und Petrographie, 3: 289–296. Paul, J., 1987. Der Zechstein am Harzrand: Querprofil über eine permische Schwelle. In: Zechstein 87 (eds. J. Kulick and J. Paul). Internationales Symposium. Exkursionsführer, 2: 193–276, Wiesbaden. Paul, J., 1993. Anatomie und Entwicklung eines permo-triassischen Hochgebietes: die Eichsfeld-Altmark-Schwelle. Geologisches Jahrbuch, A131: 197–218. Paul, J., Quast, A., Ahlborn, F., Plache, M., Reh, R., 1998. Geologie des Gipskarstgebietes zwischen Nordhausen und Stempeda (Zechstein, südlicher Harzrand). Geowissenschaftliche Mitteilungen von Thüringen, 6: 57–81. Peryt, T.M., 1994. The anatomy of a sulphate platform and adjacent Basin system in the Łeba sub-Basin of the Lower Werra Anhydrite (Zechstein, Upper Permian), northern Poland. Sedimentology, 41: 83–113. Peryt, T.M., Geluk, M., Mathiesen, A., Paul, J., Smith, K., 2010a. Zechstein. In: Petroleum Geological Atlas of the Southern Permian Basin Area (eds. J.C. Doornenbal and A. Stevenson): 123–147. EAGE Publications, b.v. (Houten). Peryt, T.M., Hałas, S., Hryniv, S.P., 2010b. Sulphur and oxygen isotope signatures of late Permian Zechstein anhydrites, West Poland: sea water evolution and diagenetic constraints. Geological Quarterly, 54 (4): 387–400. Reimann, M., 1991. Zur Vergipsung der Zechsteinanhydrite Nordwestdeutschlands. Zentralblatt für Geologie und Paläontologie, I: 1201–1210. Reimann, M., Richter, M., 1991. Lithological sequence of the Main Anhydrite (Zechstein 3) in the Piła IG1 borehole (Poland) in comparison with the normal sequence in the Hannover area (NW Germany). Przegląd Geologiczny, 39: 203–206. Renner, O., 1914. Salzlager und Gebirgsbau im Mittleren Leinetal. Archiv für Lagerstättenforschung, 13. Richter, G., 1934. Hauptanhydrit und Salzfaltung. Kali, 28: 93–95, 105–107, 122–124. Richter-Bernburg, G., 1955. Stratigraphische Gliederung des deutschen Zechsteins. Zeitschrift der Deutschen Geologischen Gesellschaft, 105: 843–854. Richter-Bernburg, G., 1985. Zechstein-Anhydrite – Fazies und Diagenese. Geologisches Jahrbuch, A85. Schachl, E., 1954. Das Muschelkalksalz in Südwestdeutschland. Neues Jahrbuch Geologie und Paläontologie, Abhandlungen, (1954): 309–394. Schachl, E., 1991. Das Steinsalzbergwerk Braunschweig-Lüneburg, Schichtlagerung in der Wurzelzone eines Salzstocks. Zentralblatt für Geologie und Paläontologie, I: 1223–1245 Seidl, E., 1914. Die permische Salzlagerstätte im Graf-Moltke-Schacht und in der Umgebung von Schönebeck a. d. Elbe. Archiv für Lagerstättenforschung, 10. Struensee, G. von, 1981. Zechstein. In: Erläuterungen zur Geologischen Karte 1:25 000, Blatt 3327 Lindwedel (ed. H.-D. Lang): 10–18. Hannover. Warren, J.K., 1999. Evaporites. Their Evolution and Economics. Blackwell, Oxford. Weber, K., 1931. Geologisch-petrographische Untersuchungen im Staßfurt-Egelner Sattel unter besonderer Berücksichtigung der Genese der Polyhalit- und Kieserit-Region. Kali, 25: 17–23, 49–55, 82–87, 97–104. Williams-Stroud, S., Paul, J., 1997. Initiation and growth of Gypsum piercement structures in the Zechstein Basin. Journal of Structural Geology, 19: 897–907. Zwanzig, W., 1928. Die Zechsteinsalzlagerstätte im oberen Allertale bei Wefensleben-Helsdorf. Kali, 22: 45–49, 62–66, 76–79, 92–94, 113–116. * E-mail: renate.paul@web.de Received: Receiced: June 6, 2014; accepted: August 30, 2014; first published online: September 16, 2014

Impressum / Datenschutz