Evaluation of controlling factors on facies distribution and ...

Evaluation of controlling factors on facies distribution and evolution in an arid continental environment: an example from the Rotliegend of the NE German Basin

H. R I E K E 1, T. M C C A N N 2, C. M. K R A W C Z Y K 3 & J. F. W. N E G E N D A N K 3

1PanTerra Geoconsultants B.V., Veerpolder 5, 2361 K X Warmond, The Netherlands (e-maib h. rieke@panterra, nl)

2Geologisehes Institut, Rheinische Friedrich- Wilhelms- Universitiit, Nussallee 8, 53115 Bonn, Germany,

3 GeoForschungsZentrum, Telegrafenberg, 14473 Potsdam, Germany

Abstract: About 3 km of core material from 14 wells together with additional data from several hundred wells across the NE German Basin (NEGB), have been investigated in order to reconstruct the facies architecture and the evolution of the Upper Rotliegend II. Special attention has also been given to the verification of various controlling factors and their influence on sedimentation in an arid continental environment. The facies architecture within the logged profiles comprises five main environments, namely braided plain, ephemeral stream floodplain, sand flat, mudflat and playa lake. The evolution can be subdivided into four distinct basin-wide correlatable periods - Parchim, Mirow, Dethlingen and Hannover formations - with each of them being characterized by a specific basin geometry and interplay of controlling factors. The deposition of the basal Parchim Formation largely took place within a tectonically created basin, whereas the facies evolution displayed an initial less-arid climatic period and later shift to an arid climate. The succeeding Mirow Formation marks the beginning of thermally induced basin subsidence. However, sedimentation itself clearly reflects a period in which the climate was relatively less arid. The overlying Dethlingen Formation was largely controlled by the increasing thermal subsidence of the basin, leading to broad extension towards the south and east. Internally, the strata can show the effects of climatic variability, depending on their position within the basin. The uppermost Hannover Formation was the product of ongoing basin subsidence, a reduction in sediment supply and an increasingly peneplaned topography. In summary, evolution of the Upper Rotliegend II within the NEGB reveals a variety of factors which have a significant influence on sedimentation, such as climate variations, the creation rate and amount of accommodation space, wind direction, sediment budget and source area lithology. An understanding of how these various factors interlink in controlling basin infill is of great significance in understanding the complex depositional history of arid continental successions.

Exclusively continental strata from recent or ancient formations have been the focus of many researchers with regard to the evolution of sedimentary basins world-wide (e.g. Leeder & Gawthorpe 1987; Blair & Bilodeau 1988; Nemec & Steel 1988; Mountney et al. 1999). These studies have tended to focus on the facies architecture, tectonic setting, sequence stratigraphy, evolution of sedimentary infill and provenance analysis. While much effort has been given to the fundamental question of the various factors controlling the sediment supply and evolution of such basins, the question as to whether synsedimentary tectonics or climate change, or a combination of both, is of greater importance to the sediment distribution, thick-

ness and resulting facies architecture, remains to be determined (e.g. Blair 1987; Frostick & Reid 1989; George & Berry 1993; Clemmensen et al. 1994; Dorn 1994; Blakey et al. 1996; Mack & Leeder 1999). The examination of the Rotliegend sediments within the Northeast German Basin (NEGB) provides an excellent opportunity to contribute to this ongoing debate.

The <2 km thick succession of Rotliegend (i.e. Upper Permian) sedimentary strata within the NE German Basin (NEGB) have been the target of extensive exploration since considerable finds of gas were made in the late 1960s, and these units represent Germany's largest hydrocarbon reservoirs (Mfiller et al. 1993). Until the early 1990s, approximately 1500 deep wells were

From: MCCANN, T. & SAINTOT. A. (eds) Tracing Tectonic Deformation Using the Sedimentary Record. Geological Society, London, Special Publications, 208, 71 94. 0305-8719/03/$15.00 �9 The Geological Society of London 2003.

at Pennsylvania State University on May 12, 2016http://sp.lyellcollection.org/Downloaded from

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72 H. RIEKE E T A L .

drilled within the NEGB and adjacent areas, with several hundred of them penetrating Rotliegend-age formations. Thus, a unique database across the entire NEGB, comprising kilometres of core material (e.g. Hoth et al. 1993), geophysical wireline logs and an extensive network of seismic profiles (particularly in NE Germany and the Altmark, see Fig. 3 for location), together with the DEKORP-BASIN 9601 profile (DEKORP-Basin Research Group 1999), has been acquired. However, detailed sedimentological studies of the Rotliegend succession, focusing on facies architecture and facies evolution within the NEGB, were lacking, since previous scientific work in the area focused mainly on the lithostratigraphy (see Plein 1995, and references therein). The stratigraphy of the Permian clastics has been mainly assumed to be controlled by a series of tectonic events, termed 'Altmark events I-IV' , which separated the sedimentary evolution of the Upper Rotliegend I! into four distinct periods (Hoffmann 1990; Gebhardt et al. 1991; Hoffmann et al. 1997). However, a detailed analysis of the sedimentary facies has never been undertaken in the region to fully establish, firstly, the precise temporal and regional development and evolution of the various continental depositional environments over time, and secondly, the interrelationship between the development of these sedimentary

units and the prevailing tectonic and other controls which were active at that time.

Our understanding of the sedimentology, facies and stratigraphy of the unfossiliferous siliciclastic Rotliegend-age formations within the Southern Permian Basin (Fig. 1) has made fundamental progress since the early 1990s (e.g. George & Berry 1993, 1997; Yang & Nio 1994; Howell & Mountney 1997; Kiersnowski 1997; Gast et al. 1998; Glennie 1998; Sweet 1999). Therefore, the aim of this paper is twofold. Firstly, a high resolution facies architecture subdivision will be presented, resulting from detailed facies interpretations. Based on these results, the evolution of the Upper Rotliegend II will be reconstructed as a series of four time slices for the NEGB. This dynamic evolution scheme will thus reveal the complexity of the interacting factors, such as tectonism, climate, sediment supply and basin subsidence, which controlled sedimentation in the area.

The database for this study consists of core material, lithological profiles and geophysical wire-line logs from about two hundred wells across the basin (Fig. 2). In order to reconstruct the facies architecture and evolution, c.3.4 km of Rotliegend core material from 14 deep wells across the northern and southeastern margins were logged in detail to determine composition, provenance, facies types, distribution and poss-

Fig. 1. Location of the NE German Basin (NEGB) within the Southern Permian Basin (after Kiersnowski et al. 1995 and Ziegler 1990).



ROTLIEGEND NE GERMANY 73

Fig. 2. Geographical map of the investigated area showing the database used in this study. (after Hoth et al., 1993; Stumm et al., 1990 and this work). Key: Am, Angermiinde; Barth, Barth; Chi, Chorin; FdlN, Friedland; Gst, Gingst; Loss, Loissin; Pnl, Penzlin; Pew, Prerow; Ric, Richtenberg; Rn, R/igen; Stav, Stavenhagen; Swan, Schwaan; Zeh, Zehdenick; ZooGs, Zootzen.

ible source areas. Additionally, predominantly unpublished extensive data-sets comprising detailed petrographical investigations and litho- facies maps from former workers provided useful background information.

Regional geology The NE German Basin is one of a series of interconnected sub-basins, together termed the Southern Permian Basin (SPB), which extended c. 1500 km from Poland in the east to England in the west (Fig. 1). The German part of the SPB

is situated between the Precambrian Baltic Shield to the north and Variscan-influenced areas to the south (Berthelsen 1992; Franke e t al. 1989; DEKORP-BASIN Research Group 1999). Three major, approximately NW-SE- striking fault zones occur in the area of the NEGB: the Caledonian Deformation Front (CDF), the Tornquist Zone (TZ), comprising the Sorgenfrei-Tornquist Zone (STZ) in the northwest and the Tornquist-Teisseyre Zone (TTZ) in the southeast, and the Variscan Deformation Front (VDF), whose exact position is still under discussion.




The present-day NE German Basin is bounded to the north by the Fyn-Mon-Arkona High which forms the eastward continuation of the Ringkobing High (Fig. 3). The southern boundary comprises the Variscan fold and thrust belt. The transition to the adjacent Polish Basin terminates the NEGB to the east, whereas the

NW German Basin represents the western limit of the study area.

In Permo-Carboniferous times the intra- continental NEGB developed in the area of the post-Variscan foreland depression (Plein 1993). In its initial phase, the collision of the northward- moving African and European plates established

Fig. 3. Geological map of the NE German Basin (NEGB) and the main tectonic elements in the region (modified from Ziegler 1990 and Plein 1995).




a dextral strike-slip regime across the region, with a predominant east-west extensional component (Arthaud & Matte 1977; Gast 1988; Ziegler 1990; Glennie & Underhill 1998). Within the NEGB, wrench-induced normal faulting along a network of NE-SW- and NW-SE- oriented tectonic lineaments took place, which has been termed 'Frankonian movements' (Fig. 3; Franke et al. 1989; Bachmann & Hoffmann 1995, 1997). This tectonic activity was partially responsible for the period of extensive magmatism across the NEGB, resulting in an up to 2000-m thick Permo-Carboniferous-age succession of predominantly calc-alkaline SiO2-rich volcanics (Benek et al. 1996). The extrusions of the effusives throughout most of the NEGB are assumed to have taken place within a short time- span between 297-302_ + 3 Ma (i.e. the magmatic

flare-up described by Breitkreuz & Kennedy 1999). Large amounts of material derived from the mantle suggest a destabilization of the lithospheric crust (Benek et al. 1996).

The cessation of tectonism and magmatic activity coincided with the onset of Rotliegend sedimentation, which was more or less continuous over a period of c.40 Ma. Therefore the Rotliegend succession within the NEGB represents the time-span from c.297 Ma (i.e. subsequent to volcanic activity) to 258 Ma (i.e. the Rotliegend-Zechstein boundary) , and has a cumulative thickness of up to 2 km (McCann 1998). Based mainly on lithostratigraphy, the Rotliegend-age strata can be subdivided into four main subgroups, namely, Altmark, Mfiritz, (for Rotliegend I) and Havel, Elbe (for Rotliegend II) (Fig. 4; Plein 1995). The latter two can be further

I R e f e r e n c e S c a l e R e g i o n a l S c a l e N E - G e r m a n y

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Fig. 4. Regional Permian stratigraphy of the NE German Basin (modified after Menning, in Plein 1995).




divided into the Parchim and Mirow formations and the Dethlingen and Hannover formations, respectively.

Initial deposition of clastics in the NEGB (i.e. Altmark and Mfiritz subgroups) was confined to a series of restricted and isolated grabens and sub-basins (e.g. Plein 1993; Rieke et al. 2001). However, little is known about the spatial distribution of these structures due to their rare occurrence in boreholes and the distinct lack of lateral control. With the exception of rare profiles which contain marine and lacustrine fossil associations, and which have been dated as Permo-Carboniferous and Lower Permian (e.g. Grfineberg Formation; Gaitzsch 1995; Schneider et al. 1995) in age, much of the Altmark- and Mtiritz-age succession is exclusively continental and its subdivision, based purely on lithostratigraphy, is questionable.

The basin-wide correlatable Saalian Uncon- formity (Fig. 4), representing a time span of uncertain age, separates the overlying Upper Rotliegend II (Havel and Elbe subgroups) from the underlying older Permian to Carboniferous strata (Fig. 4). These so-called Saalian movements reactivated the pre-existing tectonic regime with a predominant east-west extensional component (Bachmann & Hoffmann 1995). A series of roughly NE-SW-trending graben- structures was created and/or rejuvenated across the basin margins during this period (Baltrusch & Klarner 1993; Klarner 1993, this volume). At the Variscan-influenced southern margin of the NEGB, tectonism was accompanied by the extrusion of a tholeiitic to alkaline series of basaltic lavas (Marx et al. 1995).

The overlying successions of the Upper Rotliegend II are exclusively continental in character, except for some rare marine ingres- sions within the Elbe Subgroup (Plein 1995). The general lack of datable fossils precludes more definite biostratigraphic correlation. The magnetostratigraphic Illawarra reversal in the lower part of the Parchim Formation is the only chronostratigraphic time marker. This has a postulated age of c.265 Ma (Menning 1995).

In post-Illawarra reversal times, the increasing lithospheric cooling gradually extended to encompass the entire NEGB, with prograding overstepping of the basin margins (Van Wees et al. 2000). The ingression of the Zechstein Sea at 258 Ma (magnetostratigraphic date, after Menning, 1995) terminates the Rotliegend evolution within the entire NEGB.

In general, the Rotliegend environment was controlled by the palaeoposition of the Southern Permian Basin at 15~ during Permian times and by its position located in the central parts of

the continent Laurasia, several thousands of kilometres distance from the southerly located Tethyan Ocean. The climate was therefore arid to semi-arid, with a predominant palaeo-wind direction from the NE (Northern Hemisphere trade wind; Glennie 1982, 1990).

Facies interpretation A detailed interpretation and classification of the facies associations within the Rotliegend of the NEGB was possible due to the large amount of available core material. Five main facies, which are interpreted as specific environments following Hardie et al. (1978), were determined in the NEGB, namely: braided plain, ephemeral stream floodplain, sand fiat, mudflat and playa lake. Specific sedimentological processes operating within the ephemeral stream floodplain environment allowed further subdivision into distinct facies associations, which will be outlined below.

B r a i d e d p l a i n e n v i r o n m e n t

The majority of the conglomerates present within the investigated profiles occur at the very base of the Upper Rotliegend II succession and represent c.8% of the entire logged clastics. The thickness varies from several metres up to some tens of metres (e.g. 80 m in the Swan 1/76 well).

The conglomerates are predominantly clast- supported, disorganized and massively bedded, with rare weakly developed parallel bedding. Subordinate intercalations of thin beds (< 1-2 m) of matrix-supported conglomerates were noted. Open framework layers, some of which show rare poikilitic calcite cementation, also occur. The conglomerate units contain a wide range of clast sizes, ranging from single boulders to mud, although the majority are composed of a fine- to medium-sized pebble fraction. Clast shapes are generally subrounded to subangular.

The conglomerates are interpreted as having been deposited as channel bed-load within a series of fluvial channels within a braided plain environment. The subordinate matrix-supported beds were presumably deposited as the terminal lobes of dense sheet floods.

It is generally difficult to correctly determine the depositional environment of coarse-grained sediments based purely on borehole data, since the lack of boreholes precludes the establishment of the lateral geometry. Thus, it is difficult to dis- tinguish between deposits of an alluvial fan and those of a braided plain. The precise lateral geometry of the sediment bodies - in this situa- tion a decisive criterion - cannot be reconstructed solely from down-hole data. Supportive



ROTL! EGEND NE GERMANY 77

information, for example from seismic profiles, is also lacking in the NEGB, due to the absence of reflectors within the Rotliegend clastics and due to masking effects of the overburden Zechstein- evaporites (DEKORP-Basin Research Group 1999; Rieke et al. 2001). Nevertheless, coarse- grained clastic facies such as the one described are generally either derived from a tectonically controlled local alluvial fan, or they were deposited as part of a broad braided plain environment.

The conglomerates from this study show no typical sedimentological structures, for example, large-scale fining and/or coarsening upward trends, a wide spectrum of grain sizes, development of soil horizons, and changes in depositional style from sheet flow to mass flow or vice versa, which would be typical of an alluvial fan environment. The widespread occurrence of the sediments across the basin, the relatively low thicknesses (c.80 m) of the individual units, their predominant stream-flow character and the fact that fault-controlled source areas have not been definitively established, would all strongly suggest that these conglomerates should be referred to the braided plain environment.

Ephemeral stream floodplain environment

Almost all of the logged fine- to coarse-grained sandstones of fluvial origin can be grouped into the ephemeral stream floodplain environment which represents 33% of the examined profiles. The predominant sedimentation processes are channelized and unconfined ephemeral streams and sheet flows involving a mixed load of pebbles, sand and mud. The downstream reduction in the fluvial transport energy and discharge as a result of transmission loss, evaporation and the prograding diversion/ bifurcation into a distributary network of fluvial streams are key sedimentological factors for the detailed subdivision of the ephemeral stream floodplain environment. Three distinct facies associations can be distinguished, namely: proximal fluvial, medial fluvial and distal fluvial. The lateral transitions between these facies associations are gradational in character and are determined by their specific lithologies and bedding types.

Proximal fluvial facies association. A typical litholog of the proximal fluvial facies association is shown in Figure 5. The lithologies are dominated by a variety of poorly to moderately sorted coarse-, medium- and fine-grained sandstones showing sediment structures typical of the middle upper flow regime, such as medium- to

large-scale cross-sets (inclinations up to 25~ Fig. 5) or planar lamination. The sandstones are predominantly multistorey/amalgamated in character and have a thickness of up to 30 m, with internally single sets of up to 3 m. Normal grading and subordinately reverse grading occur presently within the sets usually lacking any fine- grained layers. Couplets of very poorly sorted coarse-grained sandstones and sandy mudstones were noted regularly showing intense soft- sediment deformation structures such as convolutions or single water escape structures which almost destroyed the primary fabrics. Rare intercalated muddy fine-grained sandstones (up to 1 m thick) with ripple cross-lamination or flaser structures, are indicative of lower flow regimes.

These complex successions are interpreted to represent a dense network of channelized, high- energy fluviatile streams in the proximal fluvial facies of the ephemeral stream floodplain environment. The predominantly multistorey arranged sandstone-sets bounded by erosive fluvial discordances are typical fabrics for intra-channel facies. The preservation potential for deposits of moderate to low transport energies is generally poor except for the secondary reworked couplets of sand and mud, which are interpreted as the product of overbank-flooding adjacent to the main fluvial channels.

Medial fluvia/ facies association. The lithology of the medial fluvial facies, as shown in Figure 6, is dominated by fine-grained sandstones with a grain-size spectrum ranging from mud to coarse- grained sand. The sandstones are generally moderately to poorly sorted. The sedimentary structures present - for example, ripple-cross bedding, heterolithic alternations of mud and sand, weakly horizontal bedding/lamination or structureless - are indicative of moderate to low fluvial transport energies. Fining-upward sequences with an average thickness of 2 m are common. They are usually composed of fine- grained sandy layers at the bottom which grade upwards to homogeneous mudstones or claystones at the top. Rip-up clasts within the basal parts of these fining-upward sequences are predominantly composed of mudstones while desiccation cracks are common in the mudstones at sequence tops. Poorly sorted medium- and coarse-grained sandstones are limited to rare single beds (up to 3 m thick). Internally, these sandstones exhibit weakly horizontal bedding to completely disorganized fabrics. Homogeneous, or irregular- to lenticular-bedded sandy mudstones of less than 2.5 m thickness were rarely noted.



78 H. R|EKE ETAL.

Fig. 5. Litholog from the Penzlin 1/75 well showing the proximal fluvial facies of the ephemeral stream floodplain environment. Scale: cored interval in metres.

The highly variable lithologies observed within these units may be interpreted as having been deposited within the medial fluvial facies association of the ephemeral stream floodplain environment. The predominant accumulation process is periodically unconfined sheet floods which carry mixed sand/mud loads and are indicative of an overall reduction in fluvial transport energy. The commonly occurring graded beds represent these single fluvial waning flow events and are, therefore, a very characteristic feature of this facies. However, the incision of single storey fluvial streams, related to periods of higher transport energy (i.e. flash floods after heavy rainfalls) which is likely to occur within such a

environment, is rarely noted. Rip-up clasts and desiccation cracks provide evidence of periods of subaerial exposure and indicate the ephemeral character of these streams.

The intercalation of sandy mudstones marks distinct periods of non-fluvial sedimentation within this environment. The origin of these deposits is discussed in detail in the mudflat environment section (see below).

Distal fluvialfacies association. The logged core- section (Fig. 7) shows a very typical example for the distal fluvial facies of the ephemeral stream/floodplain environment. The profiles are usually composed of interdigitated mudstones




Fig. 6. Logged section from the Stavenhagen 1/76 well illustrating the medial fluvial facies of the ephemeral stream floodplain environment. Scale: cored interval in metres.

with varying contents of sand and single fine- grained sandstone beds with a maximum observed thickness of up to 4 m. Internally, the beds include a variety of sedimentary structures, for example, small-scale ripple cross-bedding, and planar, heterolithic alternations of sand and mud, and wavy bedding. Homogeneous or completely disorganized sandstones (<0.6 m thick), are also observed. Normal grading is common, with sandstones fining upwards into mudstones or claystones. Rip-up clasts, convo- lute and water-escape structures and desiccation cracks are frequently observed.

These sediments are interpreted to represent a relatively topographically flat depositional

environment, which was subjected to episodic incursion by sandy sheet flows or mud flows of the most distal fluvial regime of the ephemeral stream floodplain environment. The surficially unconfined sheet flows rapidly wane due to transmission loss resulting in the deposition of a widespread fine-grained sandstone bed which contains a variety of sedimentary structures indicative of low-energy conditions. Inter- calated mudstones represent deposition in ephemeral freshwater lakes. The frequency of the mudstones increases downstream and is related to the decreasing periodicity of the fluvial streams. The distal fluvial facies of the ephemeral stream/floodplain environment passes laterally



80 H. RIEKE ETAL.

Fig. 7. Litholog from the Schwaan 1/76 well displaying a typical section of the distal fluvial facies of the ephemeral stream floodplain environment. Scale: cored interval in metres.

into the mudflat, sand flat or playa lake environments.

Mudflat environment

The sediments of the mudflat environment are the most frequent within the investigated profiles and represent c.45% of the logged cores. The lithologies comprise fine-grained muddy sandstones, sandy mudstones and nmdstones. Sorting is generally poor. Sedimentary structures vary markedly from irregular lenticular bedding to units which are very homogeneous and exhibit no internal structures. Boundaries tend to be diffuse rather than sharp. Isolated lenses of

either fine-grained sandstones with subrounded to rounded individual grains, or sandy mudstone, are present within the mudstones. These lenses have a mean size of 2 x 1.5 cm. Concretions of anhydrite and halite pseudomorphs were frequently noted. Desiccation cracks are rare. Fine- grained sandstone units, which are up to 2 m thick, occur sporadically within the profiles. Internally, these sandstones range from structureless, to weakly developed ripple cross-bedded or with heterolithic alternations of sand and mud.

The sediments of this environment were deposited on a flat topography where the groundwater level was either close to, or even tempor-




arily at, the surface. The semi-arid climate generated an evaporitic milieu. Thus, the main depositional process is assumed to be the accumulation of wind-blown clastic material (clay to fine-grained sand) on surficially developed efflorescent and precipitated salt crusts (cf. Goodall et al., 2000). The uppermost few centimetres of the sedimentary profile are almost completely cemented by evaporites leading to a muddy to fine-sandy substrate with embedded irregular lenses of fine-grained sand (i.e. popcorn texture). However, the salt crust itself never remains preserved and the primary sediment structures generally have a relatively low preservation potential due to very intense secondary reworking caused by deflation, halo-turbation, an oscillating water table and periodic, surficial flooding following heavy rainfall. The latter is indicated by the regular occurrence of fine- grained sandy layers (sheet flows) and by units of homogeneous to laminated claystones (<2 m thick) of highly variable colours from brown-red to green-grey which were deposited in ephemeral or perennial playa lakes. The frequent occurrence of anhydrite concretions is indicative of the presence of original surface precipitates of gypsum which were altered to anhydrite following burial.

S a n d f l a t env i ronment

Sediments belonging to the sand flat environ- merit are much less abundant than those of the mudflat, comprising approximately 9% of the logged profiles. They consist mainly of fine- grained sandstones with varying contents of mud and subordinately medium- to coarse-grained sandstones. The lithology and sedimentary structures (Fig. 8) indicate that the environment comprised a fine-grained sandy substrate with occasional mud drapes, which produced the resultant irregular wavy to crinkled laminae. Additional structures, for example, small-scale pseudo-cross-lamination, planar adhesion lamination, and vertically climbing adhesion ripples (cf. Goodall et al. 2000) were also noted. Intercalations of weakly cemented, poorly sorted, fine- to coarse-grained sandstones, showing no clear structure rarely occur. Individual bed thickness does not exceed 2 m. Anhydrite concretions, reaching a maximum size of c.10x20 cm, are rare.

In terms of their genesis, sand flat sediments are similar to those of mud flats. The predominant sedimentation process for the sand flat deposits is the accumulation of wind-blown clastic material on surficially developed salt ridges as described by Fryberger et al. (1983,

< . _

_ - - J

Fig. 8. Draft taken from the Penzlin 1/75 well indicating the characteristic textures of evaporitic and non-evaporitic sediment accumulation. Legend: Ay, concretion of anhydrite; black arrow, irregular to crinkled muddy laminae of former salt ridges; asterisk, planar adhesion lamination; white arrow, vertically climbing adhesion ripples; cross, small-scale pseudo-cross-lamination.

1984). In addition, small-scale pseudo-cross lamination, planar adhesion-lamination and vertically climbing adhesion ripples provide clear proof of subordinate non-evaporitic deposition.

In general, the sand flat environment is characterized by the input of wind-blown sand and, thus, has relatively higher accumulation rates than that of the mudflat environment. This could indicate a more proximal or marginal position of the sand flats relative to the source



82 H. RIEKE ETAL.

area. The existence of fragile, and thus rarely preserved, sedimentary structures such as pseudo- cross laminae would suggest a lower level of reworking of the sand flat sediments. Tempor- arily inundation is marked by the occurrence of poorly sorted fluvial sandstone beds of low- energy sandy sheet floods.

Playa lake environment

The successions of the playa lake environment form c.4% of the entire logged strata. Playa lake deposits mainly consist of homogeneous to laminated carbonate-rich claystones of varying colours from green-grey to red-brown. Thinly bedded to even laminated couplets of clay and silt to fine-sand were noted. Interdigitation of homogeneous to laminated claystones and sandy mudstones was also noted. Intercalations of clay laminae and clastic layers composed of fine sand to coarse sand are extremely rare. The claystones contain rare ostracode and conchostracae fossils, whereas Hydromedusae limnica (Mfiller 1978) are abundant in some profiles.

The sediments of this environment were deposited within temporary playa lakes located on the basin floor (cf. Gast 1991; Gaupp et al. 2000). Differentiation between ephemeral and perennial water bodies is rarely possible, and the term 'perennial' should only be applied to a succession comprising complete sequences of laminated claystones and evaporites (e.g. Gast 1991; Gaupp et al. 2000). The lakes within the NEGB were generally closed, with water being supplied from underground springs. Surficial clastic input by fluvial streams can thus be largely excluded owing to the generally arid climate which would have limited the lateral range of these ephemeral streams.

Upper Rotliegend H palaeogeography and basin evolution

Using the detailed facies analysis presented here, it is possible to trace the sedimentary evolution of the Upper Rotliegend II within the NEGB. Four main evolutionary stages (i.e. Parchim, Mirow, Dethlingen and Hannover formations) can be separated throughout the basin, with each of them characterizing a specific basin geometry and facies architecture.

Parchim Formation. Basin morphology at the beginning of Parchim Formation times had been largely established by the regional stress regime which comprised a major E-W-trending extensional component (Fig. 9). The main eastern

boundary of the basin is the north-south trending intrabasinal Altmark High, whereas the Wollstein High forms the limit to the SE (and partly east). Towards the north the basin is bounded by the Richtenberg High (Fig. 9). Along the basin margins several NE-trending graben-like structures developed or were rejuvenated by the existing stress regime (Baltrusch & Klarner 1993; Klarner 1993; Helmuth & Stissmuth 1993; Helmut & Schretzenmayr 1995). The main depocentre comprised two distinct sub-basins, each containing up to 600 m of sediments. These sub-basins have been interpreted as transtensional strike-slip basins (e.g. Bachmann & Grosse 1989).

Facies distribution during Parchim Forma- tion times was controlled by the tectonically generated morphology. The initial basin-wide period of sedimentation was indicative of a semi- arid climate and was marked by the extensive progradation of braided plain systems towards the sub-basin centres (Fig. 10a). The simplified palaeogeographical map shows the maximum extent of the braided plain environment. The basin margin graben systems were activated as feeder channels supplying the fluvial streams with clastic material from the surrounding Permo-Carboniferous volcanic hinterlands. Fluvial sedimentation was more active along the southern margin (residual Variscan highland areas), from where most of the sedimentary input was derived. Thus, a few wells in the area penetrated coarse-grained profiles, which show several coarsening and fining-upward cycles and strong variations in the inclination of the beds (up to 20~ These sediments might be interpreted as sheet flood-dominated alluvial fan deposits indicating a proximal deposition close to the source area.

The basin centre shows a prevailing sand flat environment. In the northwesterly sub-basin, homogeneous and laminated claystones of the ephemeral playa lake environment have also been cored.

During the succeeding arid period the sediment supply was almost cut off and the fluvial streams were restricted to thin belts across the basin margins (Fig. 10b). Most parts of the basin were covered by sand flat sediments. In the NW sub-basin, up to 70 m of evaporites (i.e. Schwerin Salina) represent this dry phase. Along the southern margin, the north-south trending Altmark High acted as a morphological barrier to sediment transport. Thus, the NE-directed palaeo-wind accumulated an extensive erg at the eastern flank of the high, comprising dunes, interdune areas and aeolian sheet sands (Kleditzsch & Kurze 1993; Helmuth & Sfissmuth 1993).




Fig. 9. Isopach map showing the distribution of the Parchim Formation (contours are in metres). Key: A, Altmark High; B, Wollstein High; C, Richtenberg High.

Mirow I~brrnation. By Mirow Formation times, thermally induced basin subsidence had led to the formation of a more uniform depositional area extending both to the east and south (Fig. 11). The basin-bounding highs were progressively eroded over time during this period. The original graben-like features are preserved along the northern and southern margins. The main depocentre is located in the northwest and contains up to 600 m of clastics.

Sediments of the Mirow Formation discord- antly overlie those of the Parchim Formation within the central parts of the basin, and Permo- Carboniferous volcanics, or locally older Carboniferous strata, along the basin margins. The lowermost boundary of this formation is a sharply developed one in almost all of the cored profiles, and can thus be easily correlated across the basin. It is characterized by the erosive occurrence of fluvial ephemeral stream floodplain sediments suggestive of a shift to a less-arid climate. The palaeogeographical map (Fig. 12a) indicates the maximum basinward progression of the fluvial belts. The fluvial-dominated strata (up

to 200 m thick) at the southern basin margin may be subdivided into proximal, medial and distal fluvial zones. Vertically, the profiles show one or two fining-upwards trends depending on their relative position within the basin. Across the northern basin margin, the older graben structures were reactivated as feeder channels. However, due to the already relatively smooth morphology, the sediments display mainly moderately to low fluvial energies and the sedimentary input was reduced. Cored profiles from the basin centre show intercalations of mudflat sediments and homogeneous claystones of ephemeral playa lakes. The latter claystones contain large quantities of Hydrornedusea, indicative of freshwater conditions.

Localized small ergs established at the southern margin suggest that the periods of arid climate were relatively short. It is also possible that the laterally restricted occurrence of these erg bodies was related to remnant topography. Coeval reduction of discharge limits the fluvial sedimentation to small belts along the margins and basin centre shows continuous mudflat facies




Fig. 10. Palaeogeographical map illustrating the facies architecture during Parchim Formation times for less arid (a) and arid (b) climate.




Fig. I 1. Isopach map showing the distribution of the Mirow Formation (contours are in metres).

(Fig. 10b). However, these periods are not correlatable, due to a low preservation potential and the unchanged sedimentation.

Dethlingen Formation. Continued thermal subsidence of the NEGB ted to further expansion towards the S and E (Fig. 13), essentially eliminating the former Richtenberg and Altmark highs, and leading to the westward connection of the basin to the NW German Basin. The depocentre during Dethlingen Formation times was located in the northwest, where up to 600 m of sediment have been drilled.

As a result of the high apparent rate of accommodation space creation during this period, the facies associations are strongly differentiated. Depending on the specific location within the basin, up to seven possibly climatic- induced cycles can be recognized (Gast & Gebhardt, 1995). Thus, the palaeogeographical maps (Fig. 14) only show the maximum extent of the various environments, and should not be considered as representative of specific spatial or temporal palaeogeographical situations.

Thermal subsidence led to the development of a groundwater-controlled perennial playa lake

within the central part of the basin. This lake extended over time to both the east and the south. Grey-green to red-brown laminated claystones represent this environment during the less arid periods (Fig. 14a). Along the southern margin, subsidence and a high sediment budget resulted in extensive progradation of the ephemeral stream floodplain environment. In contrast, the gently dipping northern margin of the NEGB was characterized by a much lower sediment budget, resulting in a weakly developed floodplain environment dominated by moderate to low transport energies. Thus, the base of the Mirow Formation corresponds with a relative retreat of the floodplain environment and a corresponding increase in mudflat sedimentation towards the basin centre.

The precipitation of lacustrine evaporites (up to a few metres thick) within the perennial playa lake environment dominated the basin centre during arid periods (Fig. 14b). Much of the basin was covered by mudftats and only narrow belts of weakly developed floodplains occur along the margins. Subordinate erg deposition, dominated by sand sheets, occurred along the southern margin (Kleditzsch & Kurze 1993). These aeolian



86 H. RIEKE ET AL.

Fig. 12. Palaeogeographical map illustrating the facies architecture during Mirow Formation times for less arid (a) and arid (b) climate.




Fig. 13. Isopach map showing the distribution of the Dethlingen Formation (contours are in metres).

facies often occur as metre-scale intercalations within the predominant fluvial facies.

Hannover Formation. Continued basin expansion towards the south and the east characterizes the final phase of Rotliegend deposition (Fig. 15). During Hannover Formation times the NEGB was now a broad uniform feature, extending both to the NW German Basin and to the easterly located Polish Basin. The main depocentre remained in the NW, with a maximum sediment thickness of up to 500 m.

The facies architecture of this final evolutionary stage in the Rotliegend of the NEGB was strongly influenced by the ongoing subsidence, the reduced topography and the consequently reduced clastic sediment supply (Fig. 16). Thus, even during less arid intervals, fluvial deposition was confined to thin belts along the basin margins (Fig. 16a). The perennial playa lake environment prograded towards the east and the south and comprised seven lake-level highstands which developed during this period (Gast & Gebhardt 1995). Cored profiles from the transi- tional areas consist of interdigitated mudflat sediments and ephemeral playa lake deposits.

During arid phases, fluvial activity ceased and mudflat deposition was extensive over large areas of the basin (Fig. 16b). The presence of more extensive evaporites (up to a few decametres thick) represent the perennial playa lake environment in the most central parts of the basin. The NE-oriented palaeo-wind led to the accumulation of extensive, sand-sheet-dominated aeolian facies along the southern margin. The ingression of the Zechstein Sea terminates the Rotliegend evolution within the entire basin.

Discussion

The evolution of the NE German Basin during Rotliegend II times and its attendant facies architecture have been outlined in detail above. From our understanding of the structural framework within which the NEGB developed, it is clear that there is only real evidence for the events which determined the actual framework of the basin itself. This series of events commenced with the major Permo-Carboniferous volcanic event and continued throughout the periods of deposition of the Altmark and Miiritz subgroups. However, the restricted sedimentary




Fig. 14. Palaeogeographical map illustrating the facies architecture during Dethlingen Formation times for less arid (a) and arid (b) climate.




Fig. 15. lsopach map showing the distribution of the Hannover Formation (contours are in metres).

record for this time period, related to the isolation of the individual basins from one another, provides evidence of a disjointed distribution pattern across the region of the NEGB. At the onset of the uppermost Rotliegend (i.e. Rotliegend II), there was a clear change in terms of the basin geometry. As noted above, during the period of deposition of the Parchim Formation, the basin comprised two distinct sub- basins, although it is not clear to what extent these basins were isolated from one another. By Mirow Formation times, however, there was a clearly unified depositional area across the entire NEGB, with highs at the margins, with sediment being sourced from these highs (and adjacent orogenic piles), and transported towards the basin centre. The distribution pattern within the basin itself broadly resembles the models of closed-basin sedimentation as outlined by Leeder & Gawthorpe (1987), albeit with the significant difference that the NEGB was not a half-graben structure. In Dethlingen Formation times, strongly increasing thermal subsidence modified the facies architecture as well as the basin geometry. In the basin centre a large climatically driven playa lake developed and the basin-

bounding highs were progressively inundated. In Hannover Formation times the pattern of sedimentation within the NEGB remained broadly similar to that of Dethlingen times, with a number of exceptions. These include the fact that the basin itself continued to grow, and also, that sediment distribution patterns were strongly influenced by the now broadly smooth topography, a resultant decrease in sediment supply and the extensive expansion of the playa lake environment across almost the entire basin.

The evolution of the Rotliegend II within the NEGB has been interpreted as being subdivided by a series of tectonic events - termed Altmark I-IV (see the introductory section of this paper for references). These events supposedly begin at the onset of the Parchim Formation (Altmark I), separate the Parchim and Mirow formations (Altmark II), Mirow and Dethlingen formations (Altmark III) and the Detlingen from the Hannower Formation (Altmark IV). It would, therefore, be expected that there should be evidence of these events both within the structural record, and more importantly in the record of the distribution of sedimentary facies around the basin itself. Periods of tectonic activity, coupled



90 H. RIEKE E T AL.

Fig. 16. Palaeogeographical map illustrating the facies architecture during Hannover Formation times for less arid (a) and arid (b) climate.




with renewed uplift, would be expected to provide new source areas, alter sediment transport directions and broadly affect the distribution of sedimentary facies (and, by extension, depositional environments) within the basin.

When the tectono-sedimentary evolution of the NEGB at this time is examined, a very different pattern is seen. The evolution of the Upper Rotliegend II within the NEGB begins with the initial transtensional-related creation of accommodation space during Parchim Forma- tion times. Despite this, sedimentation was predominantly controlled by climate variations reflecting an initial wet phase and a succeeding dry phase. Tectonic control on sedimentation is restricted to locally developed alluvial fan facies along the southern basin margin.

The subsequent basin-wide change in facies at the beginning of the Mirow Formation is characterized by the extensive progradation of fluvial facies. This is clearly related to a general change in climate to relatively less-arid conditions. Such a conclusion is supported by the fact that fluvial deposition requires both an increase in the amount and periodicity of precipitation. Additionally, no evaporites have been found within the central parts of the basin. The fluvial sandstones at the southern margin contain significant amounts of authigenic anatase, which can be interpreted in terms of a wetter climate during Mirow Formation times (Helmuth & Stissmuth 1993). The playa lake claystones contain abundant fossils of Hydromedusae limnica, indicative of freshwater conditions.

The uppermost Dethlingen and Hannover formations were strongly affected by the basin- wide thermally induced subsidence as the controlling factor for the final period of the Rotliegend. The sediment facies were very dependent on climate change. However, climate- induced cyclicities (cf. George & Berry 1993, 1997; Howell & Mountney 1997) can only be found within the most central playa lake successions. At the basin margins, except for localized areas adjacent to the Altmark High, the absence of any evidence of synsedimentary tectonics would preclude the subdivision of the various sedimentary facies, and their differentiation - both of which would be prerequisites for any climatically based correlation. In addition, the predominance of fluvial deposits at the basin margins does not allow any definitive climatic interpretations, and neither does it facilitate further refinement of the existing lithostratigraphy (Gast et al. 1998). Furthermore, the broad dish-like morphology of the NEGB (see DEKORP-BASIN Research Group, 1999) and the relative lack of any significant internal

morphology would presumably have led to intensified secondary reworking of the sediments within the basin, thus destroying the majority of the climate-change marker horizons.

The NEGB shows no evidence of significant synsedimentary tectonism, as described for the NW German Basin, the Dutch Basin (e.g. Verdier 1996) and the English Basin (e.g. George & Berry 1997). This absence presumably reflects the superior trend to increasing tectonic activities towards the west which can be explained with the beginning of the breakup of Pangea in the more western parts of the Southern Permian Basin in Upper Permian times.

The NEGB was part of the more extensive Southern Permian Basin, and directly bordered the NW German Basin to the west and the Polish Trough to the east. However, the sedimentary record of the NEGB as outlined in this study corresponds with the broad sedimentary framework of the Southern Permian Basin which developed across Northern and Central Europe. The Rotliegend of the NEGB reflects the transition from the fluvial-dominated formations, where evaporites were distinctly absent, in the easterly Polish Basin (e.g. Kiersnowski 1997; Karnkowski 1999) to the westerly NW German Basin, where fluvial facies were absent (e.g. Gast 1988; Gralla 1988). This trend, from a fluvial- dominated eastern region (i.e. wet) to an evaporite-dominated (i.e. dry) regime in the west is a reflection of climatic variations within the Southern Permian Basin.

In summary, the Rotliegend evolution within the NEGB reveals a variety of factors which have a significant influence on sedimentation, such as climate variability, the creation rate and amount of accommodation space, wind direction, sediment budget and source area lithology. Temporally changing interactions generate a depositional evolution separated into four distinct stages which are correlatable almost throughout the entire basin. The knowledge of these combinations should be strongly considered in order to understand the complex depositional history of arid continental successions.

We would to thank J. Kopp (GLA Brandenburg) and W. Von Billow, A. Janke and J. Nielson (LUNG Mecklenburg-Vorpommern) for providing access to core material, and for their help and assistance. We would also like to thank J. Graham and R. Gaupp for their helpful reviews.

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