Stephen LOUWYE, Jef DECKERS, Jasper VERHAEGEN, Rieko ADRIAENS & Noël VANDENBERGHE

A review of the lower and middle Miocene of northern Belgium

Documento adjunto(s)

Anexidades

• GB 23-3-4 Louwye et al. (7,0M)

Abstract

The stratigraphy, sedimentology and paleogeography of the lower and middle Miocene Berchem and Bolderberg Formations from northern Belgium have been extensively studied during the last decades, a.o. in the framework of doctoral research, as parts of subsurface mapping and interregional geological correlation initiatives by governmental organizations. The last formal stratigraphical revision on formation level, however, almost dates from two decades ago, notwithstanding the fact that a wealth of new data has become available. A compilation and assessment of the stratigraphical data of the lower and middle Miocene has been carried out and a refined stratigraphical framework—based on dinoflagellate cyst stratigraphy—is presented. Recommendations for the National Commission for Stratigraphy of Belgium are proposed. A new member, the Molenbeersel member, is proposed for the glauconite-bearing silts and fine sands in the upper part of the Bolderberg Formation in the Roer Valley Graben.

Tabla de contenidos

1. Introduction

1The North Sea was a semi-enclosed basin during the Neogene. The marine connection between the southern North Sea Basin and the Channel was prevented by the Weald-Artois ridge, while in the north an open marine connection with the Norwegian-Greenland Sea existed (Ziegler, 1990; Rasmussen et al., 2008; Rasmussen et al., 2010).

2Tectonic uplift of northern Belgium during late Oligocene time pushed the southern coastline of the North Sea northwards, and late Oligocene sedimentation in Belgium was limited to a thin cover of glauconitic sand in northern Belgium; it is only well developed in the subsiding Roer Valley Graben (RVG) in the very northeast (Dusar et al., 2020, this volume). At the beginning of the Miocene, during the global sea-level rise after the Mi1 glacial maximum (Miller et al., 1991), sea levels rose and northern Belgium was invaded by a marine transgression from a northern to northwestern direction (Louwye, 2005). Furthermore, Munsterman & Deckers (2020, this volume) recorded in two wells in the northeastern part of the Campine latest Oligocene – earliest Miocene (Aquitanian – early Burdigalian) deposits and proposed a transgressive phase from the Roer Valley Graben towards the Campine area.

3The marine and continental lower and middle Miocene deposits are restricted to northern Belgium and crop out in the vicinity of the city of Antwerp (Fig. 1). In the Campine area, east of Antwerp, lower and middle Miocene sediments are present in the subsurface and are covered by the late Miocene deposits of the Diest Formation (Houthuys et al., 2020, this volume). The Miocene deposits rest unconformably on Oligocene or older sediments, and the hiatus between the Oligocene and Miocene is related to the previously mentioned tectonic uplift during the late Oligocene (Vandenberghe et al., 1998). The sea invaded northern Belgium during the early Miocene from a north-northwestern direction (Antwerp Campine area) and transgressed fairly rapidly during Burdigalian – Serravallian time to the eastern Campine area. The deposition in the eastern part of the Campine area was controlled by the subsidence of the Roer Valley Graben and resulted in considerable thicknesses (>200 m; Munsterman et al., 2019).

Name	Code BGD	Code DOV	Nr		Name	Code BGD	Code DOV	Nr
Molenbeersel	049W0225	kb18d49w-B225	1		Retie	031W0243	kb17d31w-B228	13
Antwerp - Montignystraat	028W0394	kb15d28w-B448	2		Mol	031W0221	kb17d31w-B212	14
Antwerp - Van Rijwijcklaan	028W0395	kb15d28w-B449	3		Burcht outcrop		TO-20050101A	15
Berchem - Grote Steenweg	028W0397	kb15d28w-B451	4		Terhagen outcrop		TO-20050101B	16
Antwerp - Kievitstraat outcrop	028W0399	kb15d28w-B453	5		Wijshagen	048W0180	kb18d48w-B181	17
Borgerhout - Rivierenhof	028E0499	kb15d28e-B580	6		Berchem		TO-20150701	18
Zonderschoot		TO-19720101	7		Antwerp		TO-20190417	19
Heist-op-den-Berg		kb24d59e-B180	8		Maaseik	049W0220	kb18d49w-B220	20
Kalmthout	006E0110	kb7d6e-B239	9		Oelegem	029W0378	kb16d29w-B401	21
Rijkevorsel	016E0153	kb8d16e-B36	10		Mol	031W0314	ON-Mol-1	22
Oostmalle	029E0249	kb16d29e-B276	11		Weelde	008E0159	kb8d8e-B161	23
Poederlee	030W0300	kb16d30w-B315	12

Figure 1. Location of the study area with studied boreholes and outcrops (with DOV-archive numbers), distribution of the Berchem Formation, Edegem Member and Bolderberg Formation, and occurrence of Miocene sandstone boulders. A: Antwerp, B: Brussel.

4The lower and middle Miocene sediments are essentially fine-grained to coarse-grained sand, with a varying, but always considerable content of glauconite. Parts of the lower and middle Miocene are decalcified, yet calcareous (micro)fossils and macrofossils are locally abundantly present. The depositional architecture, sedimentology and fossil assemblages all indicate that sedimentation took place in a shallow marine environment.

5The lower and middle Miocene deposits are formally grouped in the Berchem Formation and the Bolderberg Formation (De Meuter & Laga, 1976; see also Laga et al., 2001) (Table 1). The former formation was deposited in northernmost Belgium, between Antwerp in the west to Lommel in the east, while the latter formation was deposited further southeast (Fig. 1). Correlation between the Berchem and the Bolderberg Formations has always been hampered by the occurrence of the late Miocene Diest Formation, deposited in a large incised valley in between the two aforementioned formations. The Berchem Formation holds the Edegem Member, the Kiel Member, the Antwerpen Member and the Zonderschot Member, while the Bolderberg Formation is divided into the Houthalen Member and the Genk Member, including the white quartz sand Opgrimbie facies (see 2.3.3.) (Table 1). The complete thickness of the Berchem Formation increases from about 30 m in the west to over 100 m in the east. The Bolderberg Formation has a maximum thickness of circa 160 m in the Roer Valley Graben in northeast Belgium (Molenbeersel borehole (BGD 049w0225, DOV kb18d49w-B225) according to Broothaers et al. (2012), truncates locally the subjacent formations and wedges out in a westward direction.

6The most recent formal revision of the lithostratigraphy of the lower and middle Miocene of Belgium already dates from four decades ago (De Meuter & Laga, 1976), and was only revised by the Stratigraphical Commission of Belgium in the beginning of this century (Laga et al., 2001). However, many recently published studies discuss facets of biostratigraphy, sedimentology, lithostratigraphy, etc. of the lower and middle Miocene (see below) and are complemented by initiatives of governmental authorities to construct detailed, comprehensive geological models. The rationale of this paper is to synthesize the available lithostratigraphical and biostratigraphical data, to review the newly available data, to evaluate the validity and status of formations and members, and to present a consistent stratigraphic framework. An overview of the discussed outcrops and boreholes can be found at https://www.dov.vlaanderen.be/data/opdracht/2020-022192.

Table 1. Lithostratigraphy of the Berchem Formation and Bolderberg Formation in northern Belgium.

2. Stratigraphy

2.1. Berchem Formation in the type area

2.1.1. The formation, sedimentology and wireline log signature

7The Berchem Formation was for the first time formally defined by De Meuter & Laga (1976) as a green to blackish, fine to medium-grained sand, often very glauconitic and with a minor clay content. Shells are abundantly present, dispersed or concentrated in massive layers. Parts of the formation, such as the Kiel Member, are locally decalcified. A distinct gravel bed of dark, rounded flint pebbles is present at the base. The type locality is Berchem (De Meuter & Laga, 1976) and the type sections of the members were temporary outcrops for the highway around the city of Antwerp (see Fig. 2 for details).

Figure 2. Geological cross section of the Berchem Formation, including the Edegem, Kiel and Antwerpen Members, in the type area. The type area is along the highway around the city of Antwerp and was defined in the temporary outcrops Antwerp - Montignystraat, Antwerp - Van Rijswijcklaan, Berchem - Grote Steenweg, Borgerhout - Rivierenhof (for location of the temporary outcrops, see Fig. 1). Hatched area: no lithostratigraphic data available. Dashed line: location and depth of profile. After Laga (unpublished, archives BGD PGL 74-103-1bis v2).

8For decades, the Edegem Member, the Zonderschot Member and the Antwerpen Member of the Berchem Formation have been extensively searched for macrofossils, especially mollusks (a.o., Glibert, 1945, 1952, 1954; Herman & Marquet, 2007). Recently macrofossils have been retrieved and studied from the Kiel Member (Everaert et al., 2019; De Schutter & Everaert, 2020, this volume). The Berchem Formation proved to hold a rich fossil fauna of marine mammals which occur in specific horizons (Misonne, 1958; Lambert, 2005, 2007, 2008; Lambert & Louwye, 2006; Louwye et al., 2010; Steeman, 2010; Dewaele et al., 2017a, 2017b). The first biostratigraphical studies of the Berchem Formation were carried out with calcareous microfossils (mainly foraminifers) retrieved from temporary outcrops made for large infrastructure works around the city of Antwerp (a.o., Hooyberghs & De Meuter, 1972; De Meuter, 1980; Hooyberghs, 1980, 1983). A biostratigraphical analysis with organic-walled dinoflagellate cysts of the members of the Berchem Formation in the type locality was carried out by Louwye et al. (2000). The latter authors analyzed samples from five temporary outcrops which were described in detail by De Meuter et al. (1976), and they correlated the deposits with the Miocene dinoflagellate cyst biozonation by de Verteuil & Norris (1996), defined in the US Atlantic Coastal Plain. The results by Louwye et al. (2000) can now be re-evaluated following the comprehensive and Sr-calibrated biozonation defined onshore and offhore Denmark (Dybkjær & Piasecki, 2010; Eidvin et al., 2014) (Fig. 3).

Figure 3. Comparison of the dinoflagellate cysts biozonation by Dybkjær & Piasecki (2010), Munsterman & Brinkuis (2004) and de Verteuil & Norris (1996). After Dybkjær & Piasecki (2010). Red lines are firm correlations (after Everaert et al., 2020, this volume).

9Based on data from Verhaegen (2020, this volume), the modal grain size of the Berchem Formation varies between 130 and 330 µm, with an average of 220 ± 56 µm. The Kiel Member and Antwerpen Member are generally slightly coarser than the Edegem Member. The modal grain size of the Edegem Member, based on 8 samples, is 190 ± 38 µm, with a clay content of 4.7 ± 3.2% and a D90 of 284 ± 97 µm. The Kiel Member, based on 9 samples, has a modal grain size of 248 ± 51 µm, a clay content of 2.5 ± 1.3% and a D90 of 404 ± 108 µm. The Antwerpen Member, based on 17 samples, has a modal grain size of 219 ± 61 µm, a clay content of 3.7 ± 2.3% and a D90 of 352 ± 102 µm (Fig. 4).

Figure 4. Grain size distribution curves for the different members of the Berchem Formation. ¹ Data from Verhaegen (2020, this volume), based on laser analyses. ² Data from Bastin (1966) based on sieving analyses. The curves based on sieving are less accurate than those based on laser analyses as less grain size intervals are defined during sieving. For Bastin (1966) the following intervals were measured: 0 – 44 – 62 – 88 – 124 – 175 – 250 – 350 – 490 – 600 µm. Data points are indicated on the curves. ³ Data from Huyghebaert & Nolf (1976), also based on sieving analysis. Following intervals were measured: 0 – 2 – 10 – 20 – 50 – 63 – 88 – 125 – 177 – 250 – 354 – 500 – 600 µm. Data points are indicated on the curve.

10Based on clay mineralogy, no distinction can be made between the members of the Berchem Formation, with smectite being the dominant clay mineral (Adriaens, 2015). All lower and middle Miocene marine units are rich in glauconite. The highest glauconite contents are noted in the Antwerpen Member, with values over 50% (see below). Bulk mineralogical data are available for the fraction <32 µm (Adriaens, 2015). In this fraction, the sediments of the Berchem Formation are dominated (30–90%) by dioctahedral Al-rich clays (mainly smectite and interstratified illite/smectite) and Fe-rich clay (glauconite minerals). Both K-feldspar and plagioclase are present (<15%). The carbonate content is highest in the Edegem Member (15–20%) and lowest in the Kiel Member (<5%). Depending on the fossil species, calcite or aragonite are present. Siderite can occur as secondary mineral.

11The Berchem Formation is characterized by a large amount of epidote, amphiboles and garnet, making up on average more than 50% of the transparent heavy mineral composition (Verhaegen et al., 2019; Verhaegen, 2020, this volume). The values for these mineral groups combined are the highest of any Belgian Neogene formation. The highest content (36%) of epidote and amphibole, related to a northern marine sediment input, is reached in the Antwerpen Member (Verhaegen, 2020, this volume). The Berchem Formation is relatively rich in CaO and Na₂O compared to the other Neogene units, which may be related to the unweathered nature of these sediments and their high smectite clay content, in comparison to other Belgian Neogene units. The Berchem Formation is also relatively rich in K₂O, MgO, P₂O₅ and Al₂O₃, all components being related to the high glauconite content (Verhaegen, 2019). The elevated P₂O₅ in the bulk analysis of glauconite pellets of the Berchem Formation could be related to the common presence of phosphatic pebbles and bone fragments; in this respect it is remarkable that glauconite pellets in the Berchem Formation generally have a P₂O₅ content >0.15% with outliers >1% compared to values <0.10% for Eocene and Paleocene glauconite pellets, including authigenic glauconites from the Lutetian ‘bande noire’ having on average 0.04% ^P₂^O₅ ^content. A higher P₂O₅ content can be observed in the overlying Neogene units as well, likely due to continued reworking of lower Miocene glauconites (Adriaens, 2015; Verhaegen, 2019).

12On wireline log data, the Berchem Formation is characterized by high gamma ray (GR) and moderate resistivity values. While the gamma ray values can be similar to those of the underlying clays or sandy clays of the Boom and Eigenbilzen Formations, the resistivity values of the sand of the Berchem Formation are markedly higher. The lower boundary of the Berchem Formation therefore coincides with a strong upward increase in resistivity. Compared to the Berchem Formation, the overlying Diest Formation is characterized by lower gamma ray and higher resistivity values which agree with the smaller amounts of glauconite and an overall coarser grain size, except for the Dessel Member (Adriaens, 2015). The boundary between the Berchem Formation and Diest Formation can therefore be positioned at an upward decrease in gamma ray values and increase in resistivity values. Generally, the highest gamma ray values are situated in the upper part of the Berchem Formation (Fig. 5).

Figure 5. The characteristic log-signature of the Berchem Formation (not in the type section) in the Oelegem borehole (DOV kb16d29w-B401). The members of the Berchem Formation are tentatively interpreted. The interpretation of the Edegem Member is based on the brighter color of the sediments (from 52 m onwards) and the description of gray-green clayey sands (from 56–60 m depth), the Kiel Member on the indication of decalcification (between 48–52 m depth), and the Antwerpen Member on the dark green to black color and very glauconite-rich nature of the sediments.

2.1.2. Edegem Member

13Nyst (1861) first observed the Edegem Member and described the unit as ‘Sables d'Edeghem à Panopea menardii’ in a quarry near Antwerp. The Edegem Member was regarded as the lower part of a twofold middle Miocene unit, named the ‘Anversien’ (Cogels & Van Ertborn 1879; de Heinzelin, 1956). This view was also adopted during the International Neogene Symposium in 1961 (Tavernier & de Heinzelin, 1963). The base of the Edegem Member is formed by the Burcht Gravel consisting of dark rounded flint pebbles, shell fragments, shark teeth and bone fragments. Reworked foraminifers, septaria and glauconite provide evidence for substantial reworking of sediment from the underlying Oligocene Boom Formation (Vandenberghe et al., 1998). The Edegem Member consists of green to grayish-green fine-grained, clayey and glauconitic sand. Large numbers of mollusks are dispersed throughout the sediment (De Meuter & Laga, 1976). In general, the granulometry of the Edegem Member displays an upwards coarsening signature as observed in two locations in the Antwerp area (Bastin, 1966), corroborated by the log-interpretation of the Edegem Member in borehole Oelegem (Fig. 5). Grain-size distribution curves of glauconite are similar to the quartz grain size distribution curve. This indicates that the glauconites of the Edegem Member are reworked and were transported together with the quartz grains (Adriaens, 2015). The glauconite content of the Edegem Member is smaller than in the Antwerpen Member (Adriaens, 2015), which explains the paler color of sediments of the former compared to the latter. The Edegem Member reaches its largest thickness of about 12 m just east of the city of Antwerp (Deckers et al., 2019).

14The first biostratigraphical analysis of the Edegem Member was carried out with planktonic foraminifera by Hooyberghs & De Meuter (1972) in unspecified temporary outcrops in the Antwerp area. The presence of a considerable number of reworked foraminifera led to an erroneous correlation with the middle Oligocene Globerigerina ampliapertura N1/P20 Zone of Blow (1969). Hooyberghs (1983) revised the assessment through a study at Terhagen where the presence of Globorotalia kugleri and Globogerinoides primordius led to a revised correlation with the Aquitanian Zone N4 of Blow (1969). Hooyberghs & Moorkens (1988) presented in a synthetic paper a correlation with the planktonic foraminifera NPF11 Globigerinoides primordius Zone defined by Spiegler et al. (1988), also indicating an Aquitanian age. The biostratigraphical analysis of the planktonic foraminifera by Hooyberghs (1996a) from a temporary outcrop at Wilrijk confirmed the Aquitanian age of the Edegem Member, although Globorotalia kugleri was not recorded. Doppert et al. (1979) placed the benthic foraminifera from the Edegem Member in the lower Miocene BFN1 Trifarina gracilis rugulosa – Elphidium ungeri Zone, an assemblage zone erected by the latter authors and based on the work by De Meuter & Laga (1976) in a temporary outcrop in Antwerp. The compilation by Willems et al. (1988) indicates a correlation with the benthic foraminifera Zone B7, a zone of earliest Miocene age, not further specified. Calcareous nannoplankton of the Edegem Member was studied by Martini & Müller (1973) and correlated to the mid-Burdigalian NN3 Zone of Martini (1971). According to Verbeek et al. (1988) the Edegem Member correlates to the Discoaster druggii NN2 Zone and the Sphenolithus belemnos NN3 Zone defined by Martini (1971). The correlation is indicative for an Aquitanian to Burdigalian age. Gaemers (1988) examined Gadidae otoliths and placed them in his Colliolus johanetta Zone11. Rare Bolboforma rotundata were recorded in the Edegem Member in temporary outcrops in the Antwerp area, and point to an age between 23.8 Ma and 18 Ma according to Spiegler (2001), i.e. latest Chattian to early Burdigalian. Janssen & King (1988) reviewed previous pteropod collections from the Edegem Member and proposed a correlation with the early Miocene Pteropod Zone 18 based on the occurrence of Vaginella austriaca. Janssen (2001) suggested an age no older than late Burdigalian for the Edegem Member.

15The Edegem Member from the temporary outcrops in Antwerp Montignystraat (BGD 028W0394, DOV kb15d28w-B448) and Van Rijswijcklaan (BGD 028W0395, DOV kb15d28w-B449) (Fig. 2, see also De Meuter et al., 1976) holds the dinoflagellate cysts Exochosphaeridium insigne species and Cordosphaeridium cantharellus, indicative of a correlation of the Edegem Member with the Cordosphaeridium cantharellus Zone (Dybkjær & Piasecki, 2010) (Fig. 6). The new Sr-dating of dinoflagellate cyst bioevents by the latter authors allows to constrain the age of the Edegem Member between 19 Ma and 18.4 Ma (early Burdigalian).

16Glauconite grains pose particular problems for radiometric dating because of their complicated origin and slow early evolution, and therefore are called sub-authigenic by Dickin (2005). Also, glauconite pellets can be reworked at a considerable scale as was demonstrated for the Tortonian Diest Formation in the Campine area (Vandenberghe et al., 2014). Still, many attempts using glauconites for dating strata have been undertaken with a varying success rate (Odin, 1982; Amorosi, 1997; Dickin, 2005). Radiometric glauconite dating of the Miocene deposits of northern Belgium was also attempted (Odin et al., 1969, 1974; Keppens, 1981; Keppens & Pasteels, 1982) and the results were summarized by Odin & Kreuzer (1988) in the IGCP 124 North Sea stratigraphy review volume (Vinken, 1988). The reliability of the obtained ages was evaluated through their compatibility with established biostratigraphical data of the strata and through the similarity of the ages obtained by the couples K-Ar and Rb-Sr in the same stratigraphic level. Applying these criteria, the glauconites in the Edegem Member indicate K-Ar ages between 21.3 Ma and 26.6 Ma (Aquitanian – Chattian) while the Rb-Sr ages between 24 and 30 Ma (Chattian – Rupelian) are considered a result of reworking, a conclusion already reached in an earlier paper by Odin et al. (1969) for a sample from the Edegem Member at Terhagen.

Figure 6. Stratigraphic position of the lower and middle Miocene lithostratigraphic units (members) in northern Belgium. The correlation to chronostratigraphy is based on the dinoflagellate cyst zonation of Dybkjær & Piasecki (2010). Correlation of the standard nannoplankton zonation (Martini, 1971) with the dinoflagellate cyst zonation is after Dybkjær & Piasecki (2010). Solid line between zones: lower or upper boundary was recognized. Dashed lines: lower or upper boundary was not recognized or unsure. ?: inferred stratigraphic range. *: stratigraphic position after Munsterman & Deckers (2020, this volume). The position of the members versus sequence stratigraphy of Rasmussen (2004a, b) is indicated.

2.1.3. Kiel Member

17The Kiel Member was for the first time observed by Vanden Broeck (1874) during the construction works for the fortresses around the city of Antwerp. The latter author recognized already the relation with the subjacent Edegem Member and described the Kiel Member then as ‘Partie supérieure altérée des sables à Panopées du Kiel’. The name was never really in use and the sandy Kiel unit was even not discussed during the International Neogene Symposium in 1961 (Tavernier & de Heinzelin, 1963).

18The Kiel Member was formally re-introduced by De Meuter & Laga (1976) and described in the type locality Kiel (a suburb of the city of Antwerp) as a non-fossiliferous (i.e. decalcified), medium fine-grained to coarse-grained sand, very rich in glauconite, sometimes concentrated in patches. Thin layers of coarser sand grains are occasionally present at the base of the unit. This facies occurs in the south and central part of the city of Antwerp. To the north and east of Antwerp, however, this member becomes fossiliferous, and renders the distinction with the superjacent Antwerpen Member difficult or even impossible (De Meuter & Laga, 1976). The validity of this facies as a separate member was questioned (Louwye et al., 2000). Everaert et al. (2020, this volume) studied several temporary outcrops of the Kiel Member in Antwerp and could distinguish the Kiel and Antwerpen Members by a slight but marked color difference due to a somewhat lower clay and glauconite content and a coarser sand fraction in the Kiel Sand Member.

19The Kiel Member was analyzed biostratigraphically with dinoflagellate cysts by Louwye et al. (2000) in temporary outcrops around Antwerp, namely Van Rijswijcklaan and Grote Steenweg (BGD 028W0397, DOV kb15d28w-B451) (Fig. 2, see also De Meuter et al., 1976). The recovered dinoflagellate cyst assemblages had a low diversity and poor to medium preservation, contrary to the subjacent and superjacent members where diverse and well-preserved assemblages were recorded. The presence of Exochosphaeridium insigne, the marker species of the eponymous zone of Dybkjær & Piasecki (2010), in the lower part of the Kiel Member in the Van Rijswijcklaan combined with the absence of Cordosphaeridium cantharellus, refers the lower part of Kiel Member to the (lower part of the) Exochosphaeridum insigne Zone of mid-Burdigalian age (18.4 Ma – 17.8 Ma). The upper part of the Kiel Member in the Grote Steenweg outcrop belongs to the superjacent Cousteaudinium aubryae Zone defined by the first occurrence of the eponymous species to the first occurrence of Labyrinthodinium truncatum. The latter species is not recorded in the upper part of the Kiel Member. The Cousteaudinium aubryae Zone has a late Burdigalian age (17.8 Ma to 15.97 Ma). The Exochosphaeridum insigne Zone was also recorded by Louwye et al. (2000) in the lower part of the Kievitstraat outcrop more to the north (BGD 028W0399, DOV kb15d28w-B453) (see also De Meuter et al., 1976), and is immediately covered by the Langhian Labyrinthodinium truncatum Zone of Dybkjær & Piasecki (2010) (see below). The Cousteaudinium aubryae Zone is thus lacking at the Kievitstraat ourcrop, and this implies a local hiatus of circa 1.8 Ma. It is worth mentioning that all sediments at this site were lithostratigraphically interpreted by De Meuter et al. (1976) as belonging to the Antwerpen Member. The Kiel Member was deposited between 18.4 Ma and 15.97 Ma (middle to late Burdigalian) (Fig. 6).

20In their study of the stratigraphy and the macrofossils of three temporary outcrops of the Kiel Sand in the Antwerp area, Everaert et al. (2020, this volume) also report on the dinoflagellate cysts assemblages. The relative dating with dinoflagellate cysts, albeit following the biozonation by de Verteuil & Norris (1996), indicate the presence of the DN2 and DN3 Zones and is in agreement with the above-mentioned zonation by Dybkjær & Piasecki (2010) (Fig. 3). The dinoflagellate cyst analysis of a sample from the very base of the Kiel Member however pointed to a late Aquitanian age. The cause for this deviating inferred age of this sample needs further elucidation. Age dating of glauconites in the Berchem Formation shows that reworking is not uncommon even in the Antwerpen Member (see below). This recent study on the Kiel Member confirms the hiatus between the Kiel and Antwerpen Members expressed by the rapid disappearance of dinoflagellate cyst biozone DN3 in northern direction (Everaert et al., 2020, this volume, fig. 11); these authors even suggest to locate the Early Miocene Unconformity (EMU) of Munsterman et al. (2019) at this level.

21As is the case for the Edegem Member, the Kiel Member contains glauconite which, based on radiometric dating and grain-size distribution curves, are presumed to be reworked (Odin et al., 1974; Vandenberghe et al., 2014; Adriaens, 2015). The radiometric datings further show divergence between K-Ar ages (23 to 25.3 Ma; Chattian) and Rb-Sr ages (30 Ma; Rupelian) (Odin & Kreuzer, 1988).

22Based on a gravel bed at the base of the Kiel Member, observed only in one outcrop, and a thin layer of coarse sand, Vandenberghe et al. (1998; 2004) interpreted the Edegem Member and Kiel Member as two separate incomplete sequences resulting from a competing tectonic uplift and a rising sea level. The Edegem Member displays a coarsening upwards signature in the grain size (Fig. 5), suggestive of a highstand systems tract. The log-signature suggests that maximum regression is represented by the coarser Kiel Member and a subsequent transgression marked the transition towards the Antwerpen Member. No distinct break in sedimentation can be deduced from dinoflagellate cyst biostratigraphy, indicating that the Kiel Member was deposited only slightly later than the Edegem Member (Louwye, 2000; Louwye, 2005). Taking into account the age constraints as derived above, the Edegem Member and Kiel Member could approximately be correlated to the Bur 2 and Bur 3 sequences as figured by Hardenbol et al. (1998, chart 2). A correlation with the sequence stratigraphic scheme by Rasmussen (2004a, 2004b), defined in Demark, proved more difficult given the absence of a precise dating of the sequence boundaries. The Edegem Member can maybe be correlated with the highstand system tract of their sequence C, while the Kiel Member would then be correlated to sequence D.

2.1.4. Antwerpen Member

23The Antwerpen Member was observed for the first time by Nyst (1845) during the works for the fortifications around Antwerp and was called ‘Sable noir du Fort d’Herenthals’. Later, Vanden Broeck (1874) renamed the unit as ‘Sables à Pectunculus pilosus’. The Antwerpen Member was for the first time formally described by de Heinzelin (1956) and regarded as the upper part of the middle Miocene ‘Anversien’. This view was later adopted during the International Neogene Symposium in 1961 (Tavernier & de Heinzelin, 1963) and the definition of the member was emended by De Meuter & Laga (1976).

24The Antwerpen Member consists of dark green to blackish, medium fine-grained, slightly clayey and very glauconitic sand (De Meuter & Laga, 1976). Characteristic are shell layers of a.o. Glycymeris baldii with a varying thickness. Layers with phosphatic concretions, friable sandstones, bones and shark teeth are observed towards the base of the member. The latter authors stipulate that no clear basal gravel is present. The average glauconite content reaches 47% (Fig. 7), which is the highest amount in any unit in the Campine Basin (Adriaens, 2015). In contrast to the Edegem Member and the Kiel Member, the Antwerpen Member contains mostly authigenic glauconite (Vandenberghe et al., 2014; Odin & Kreuzer, 1988).

Figure 7. Pelletal glauconite contents (in wt%) of samples of the Edegem, Kiel and Antwerpen Members of the Berchem Formation. Pelletal glauconite was isolated from the bulk sediments by magnetic separation after washing and pre-sieving at 32 µm. The pelletal glauconite content of three Oligocene Voort Formation samples was added for comparison.

25The Antwerpen Member was examined for planktonic foraminifera by Hooyberghs (1983) in the temporary outcrop Kievitstraat, and he proposed a correlation with the N6 Globigerinoides trilobus Zone (late Burdigalian) to the N9 Globorotalia peripheroronda Zone (Langhian) of Blow (1969). Hooyberghs (1983) studied a poorly preserved foraminifera assemblage from the Antwerpen Member and noted that the planktonic foraminifera from the lower part of the member are distinctly older than those from the upper part. Hooyberghs & Moorkens (1988) proposed in a review paper a correlation with the NPF12 Globogineroides trilobus Zone to the NPF13 Globorotalia praescitula Zone defined by Spiegler et al. (1988), also pointing towards a late Burdigalian to Langhian age. They furthermore state that the base of the Serravallian NPF14 Zone could be present. Willems et al. (1988) attributed the benthic foraminiferal assemblage of the Antwerpen Member to the B7 Zone of the IGCP 124 Working Group. Based on benthic foraminifera, De Meuter & Laga (1976) correlated the Antwerpen Member from the Rivierenhof outcrop (BGD 028E0499, DOV kb15d28e-B580) with the mid-Miocene Uvigerina tenuipustulata – Elphidium inflatum Assemblage Zone. Doppert et al. (1979), based on De Meuter & Laga (1976), formalized the latter zone as the BFN2 Uvigerina tenuipustulata – Elphidium inflatum Zone. The calcareous nannoplanton from a temporary outcrop at Borgerhout led Martini & Müller (1973) to propose a correlation with the NN4 Zone (late Burdigalian to Langhian). Verbeek et al. (1988) confirmed this attribution in a review paper.

26Dinoflagellate cysts from the Antwerpen Member were studied in the three temporary outcrops Grote Steenweg, Kievitstraat and Rivierenhof (Louwye et al., 2000) (Fig. 2, see also De Meuter et al., 1976). The Labyrinthodinium truncatum Zone (Dybkjær & Piasecki, 2010), defined from the lowest occurrence (LO) of the eponymous species to the LO of Unipontidinium aquaeductus and dated as early Langhian (15.97 Ma to 14.8 Ma), was recognized in all three outcrops. The superjacent Unipontidinium aquaeductus Zone, defined from the LO of the eponymous species to the LO of Achomosphaera andalousiensis and dated as early Langhian to early Serravallian (14.8 Ma to 13.2 Ma), is only present in the Rivierenhof outcrop. The uppermost part of the Antwerpen Member in the Rivierenhof outcrop holds both Achomosphaera andalousiensis and Cannosphaeropsis passio and can thus be allocated to the Achomosphaera andalousiensis Zone dated between 13.2 Ma to 12.8 Ma (early to mid-Serravallian) (Fig. 6). The Antwerpen Member was thus deposited between 15.97 Ma and 12.8 Ma (Langhian – mid-Serravallian).

27The radiometric datings of glauconites from the Antwerpen Member in temporary outcrops along the highway around the city (Fig. 2) give a K-Ar age of 20 Ma (Burdigalian) and a Rb-Sr age of 18.5 Ma to 21.5 Ma (Odin & Kreuzer, 1988). In the present time scale (ICS chart 2020/03) the Antwerpen Member would be of latest Aquitanian to mid-Burdigalian age. This age assessment contrasts with the biostratigraphical age interpretation indicating a Langhian to mid-Serravallian age. It should be noted that the Antwerpen Member is notoriously rich in glauconite pellets with many samples between 50% and 60% pellets and some samples with a higher pellet content of more than 80% (Bastin, 1966). The comparison between the grain shapes and the size distribution shapes of glauconite pellets and quartz grains in samples of the three members of the Berchem Formation confirms the reworking of the pellets in the Edegem Member and Kiel Member and the authigenesis in the Antwerpen Member (Vandenberghe et al., 2014; Adriaens, 2015). The obvious discrepancy between the radiometric and biostratigraphical ages indicates that the authigenic glauconites in the Antwerpen Member also contain reworked pellets, shifting the radiometric age to somewhat older ages.

28The Antwerpen Member is the third incomplete sequence of the lower-middle Miocene, due to continuing tectonic uplift of the Brabant Massif to the south. The presence of authigenic glauconite, phosphate pebbles and hardgrounds near the base of the Antwerpen Member are interpreted as an indication of a new transgressive phase, i.e. a transgressive surface (see also fig. 11 in Everaert et al., 2020, this volume). Each member of the Berchem Formation was thus considered to represent the transgressive and/or highstand phase of a different sequence and the base of the Antwerpen Member was correlated to the Bur 5/Lan 1 (16.5 Ma) sequence boundary by Vandenberghe et al. (1998; 2004). Taking into account the biostratigraphic age range for the deposition of the Antwerpen Member as discussed above, the sedimentation of the Antwerpen Member took place during three sequences as defined by Hardenbol et al. (1998, chart 2): Bur 5/Lan 1, Lan 2/Ser 1 and Ser 2. The boundary of sequence E of Rasmussen (2004a, 2004b) (see Fig. 6) is interpreted by the latter author as corresponding to a major transgression in the North Sea Basin and correlated to the mid-Miocene unconformity (MMU). The lower part of the sequence reflects a major transgression and resulted in the deposition of glauconite-rich sediments, similar to the Antwerpen Member. In the Belgian and Dutch glauconite-rich Neogene sections (see also Munsterman et al., 2019) the MMU is however situated at a major hiatus between the Berchem and Diest Formations at the turn of the Serravallian to the Tortonian.

2.1.5. Zonderschot Member

29The Zonderschot Member occurs in the area of Heist-op-den-Berg in the south of the Berchem Formation outcrop area. The Zonderschot Member was first described during construction works for a gas pipeline and formally defined by De Meuter & Laga (1976) as a dark green, rather fine-grained, clayey, slightly ligniferous, very glauconitic sand. The micaceous sediment is very rich in homogeneously dispersed shells (De Meuter & Laga, 1976). The formation rests unconformably on the lower Oligocene Boom Formation and is overlain to the northeast and east by the upper Miocene Diest Formation. The Zonderschot Member wedges out to the south. The unit was described in detail in a 7 km long trench by Huyghebaert & Nolf (1979). Based on the analyses of these authors, the Zonderschot Member is finer grained than the other members of the Berchem Formation, with a mode between 125 and 177 µm and a higher clay content of approximately 12% (Fig. 4).

30Hooyberghs (1980) recognized in a temporary outcrop at Heist-op-den-Berg in the Zonderschot Member the regional Globigerinoides trilobus trilobus/Globigerinoides altiaperturus Biozone (Blow, 1969), a zone correlated later by Hooyberghs (1996b) to Biozone N6 or Biozone N7, which would then indicate at least a Burdigalian age for the deposits. De Meuter & Laga (1976), Doppert et al. (1979) and De Meuter (1980) examined the benthic foraminifera from the Zonderschot Member in a temporary outcrop and correlated the sand with the middle Miocene Uvigerina tenuipustulata – Elphidium inflatum BFN2 Zone.

31The calcareous nannoplankton from the Zonderschot Member indicates the presence of the NN4 Zone, and a late Burdigalian to early Langhian age could be inferred (Verbeek et al., 1988). Nolf (1977), Huyghebaert (1978), and Huyghebaert & Nolf (1979) studied the teleost otoliths from the type-area of the Zonderschot Member and inferred deposition during middle Miocene times. Gaemers (1988) correlated the Zonderschot Member with otolith Zone 12 (German regional stages Oxlundian, late Hemmoorian or late Burdigalian, earliest Langhian). Spiegler (2001) recorded the Bolboforma rotundata Zone in the Zonderschot Member and inferred an early Miocene age.

32Louwye (2000) analyzed the dinoflagellate cysts of the Zonderschot Member from two locations in the Zonderschot area (DOV TO-19720101 and DOV kb24d59e-B180) and correlated the deposits with the Distatodinium paradoxum DN4 Zone by de Verteuil & Norris (1996). The Langhian Labyrinthodinium truncatum Zone by Dybkjær & Piasecki (2010), defined in the Danish part of the North Sea Basin, is correlatable with the latter zone, but is more detailed in terms of the assemblage (Fig. 6). The age of the zone is early Langhian (15.97 Ma to 14.8 Ma). The radiometric dating of the Zonderschot Member based on glauconites is considered as reliable with an age of 15.5 Ma (early Langhian) (Odin & Kreuzer, 1988).

33The Zonderschot Member is coeval with the lower part, and the lower sequence (Bur 5/Lan 1), of the Antwerpen Member (Louwye, 2000), and differs from the latter by the presence of mica and lignite fragments, a statement previously advanced by Huyghebaert & Nolf (1979).

2.2. The Berchem Formation outside the type area

34The Berchem Formation was recovered in the Campine area, i.e. the area north and east of Antwerp, in numerous boreholes, drilled a.o. by the Geological Survey of Belgium (Fig. 1). In the records of the Geological Survey of Belgium, the lower and middle Miocene deposits are usually referred to as Berchem Formation with only sporadic reference to members, (e.g. “Sands of Antwerpen s.l.” in the Poederlee borehole—see below; “Antwerpen sands” and “Edegem sands” in the Kalmthout borehole—see below). The Berchem Formation was analyzed biostratigraphically with dinoflagellate cysts in eight cores from the Campine area, from which six by Louwye (2005) at Kalmthout (BGD 006E0110, DOV kb7d6e-B239), Rijkevorsel (BGD 016E0153, DOV kb8d16e-B36), Oostmalle (BGD 029E0249, DOV kb16d29e-B276), Poederlee (BGD 030W0300, DOV kb16d30w-B315), Retie (BGD 031W0243, DOV kb17d31w-B228) and Mol (BGD 031W0221, DOV kb17d31w-B212) (Fig. 8), and two by Munsterman & Deckers (2020) at Mol (ON-Mol-1, BGD 031w0314, DOV ON-Mol-1) and Weelde (BGD 008E0159, DOV kb8d8e-B161). Two of these cores, the Rijkevorsel core and the Poederlee core were biostratigraphically analyzed with foraminifera and were reported on in the logs (unpublished data by P. Laga).

Figure 8. Distribution of the lower and middle Miocene dinoflagellate cyst zones in the Campine area in a NW-SE transect, after Louwye (2005), and based on the dinoflagellate cyst zonation by Dybkjær & Piasecki (2010). Foraminifera zonation after De Meuter & Laga (1976), based on unpublished data from the Geological Survey of Belgium for the Poederlee borehole (DOV kb16d30w-B315 and Rijkevorsel borehole (DOV kb8d16e-B36). Hatched interval: not studied. See Fig. 1 for locations of the boreholes.

35Munsterman & Deckers (2020) recorded the oldest Miocene (early Aquitanian) at the very base of the Weelde borehole in one sample (Fig. 1). The oldest Miocene deposits noted by Louwye (2005) are present in the Kalmthout well in the Campine area, the Antwerp area and more to the south in the Burcht (DOV TO-20050101A) and Terhagen area (DOV TO-20050101B) (Fig. 1), and hold the early Burdigalian Cordosphaeridium cantharellus Zone (19 Ma to 18.4 Ma, see above). In the Antwerp area, the Cordosphaeridium cantharellus Zone is recognized in the Edegem Member. The superjacent mid-Burdigalian Exochosphaeridium insigne Zone (18.4 Ma to 17.8 Ma) has a large geographical extent and is present from the Kalmthout well in the north to Terhagen in the Antwerp area in the south (i.e. the southernmost extent of the Miocene), and to the east as far as Poederlee (Fig. 1). The late Burdigalian Cousteaudinium aubryae Zone (17.8 Ma to 15.97 Ma) is present in all wells in the central to eastern part of the Campine area as far as Retie, and is particularly well developed in the Oostmalle well with a thickness of circa 12 m. In the Antwerp area, both the Exochosphaeridium insigne Zone and the Cousteaudinium aubryae Zone are recognized in the Kiel Member. The lower Miocene foraminifera Zone Trifarina gracilis rugulosa – Elphidium ungeri was recognized in the Rijkevorsel and Poederlee wells at comparable depths of the E. insigne and C. cantharellus Zones.

36The superjacent early Langhian Labyrinthodinium truncatum Zone (15.97 Ma to 14.8 Ma) and early Langhian to early Serravallian Unipontidinium aquaeductus Zone (14.8 Ma to 13.2 Ma) are present in the entire Campine area with moderate thickness but are best developed in the Oostmalle well with a thickness of 4 m and 3 m, respectively. The youngest mid-Miocene biozone is the early to mid-Serravallian Achomosphaera andalousiensis Zone (13.2 Ma to 12.8 Ma) in the Kalmthout and Retie wells, and does not exceed 1.5 m. In the type area of the Berchem Formation, the mid-Miocene Labyrinthodinium truncatum, Unipontidinium aquaeductus and Achomosphaera andalousiensis Zones are recognized in the Antwerpen Member. The dinoflagellate cyst zonation corroborates the presence of the mid-Miocene foraminifera Zone Uvigerina tenuipustulata – Elphidium inflatum Zone in the Rijkevorsel and Poederlee wells at comparable depths of the above-mentioned dinocyst zones.

37The Miocene transgression thus entered northern Belgium from a north to northwestern direction. Early Aquitanian deposits are recorded in the base of the Weelde borehole in the eastern Campine area near the border with The Netherlands. The oldest deposits of the Berchem Formation in the western Campine area are recorded in the Kalmthout area and are coeval with the Edegem Member of the type area. It is only during mid- and late Burdigalian time that the sea transgressed to the east as far as Retie, and deposited sediments coeval with the Kiel Member of the type area. The thickest Burdigalian deposits are present in the Oostmalle area. Langhian and early Serravallian deposits, coeval with the Antwerpen Member in the type area, have a fairly constant and moderate thickness ranging between circa 7 m and 4 m in the Campine area.

2.3. Bolderberg Formation

2.3.1. The formation, sedimentology and wireline log signature

38The Bolderberg Formation was described for the first time as ‘Boldérien’ by Dumont (1849) who assigned a Miocene age to the unit. Dumont (1849) already recognized the twofold division: the Elsloo gravel bed, followed by a marine, glauconitic lower unit and an upper lignitic, sandy unit which he considered as fluviatile in origin. The Bolderberg Formation was subsequently the subject of many studies, and the stratigraphic position of the formation switched from the Miocene to the Pliocene, and back to the Miocene. A key observation was made by Halet (1935) during the digging of a mine shaft at Houthalen in the coal mining district of the Campine area, where the superposition of the lower glauconitic, marine sand and the superjacent non-marine sand was observed for the first time. Halet (1935) advanced furthermore a correlation of the marine ‘Boldérien’ with the ‘Anversien’ (see above), and indirectly attributed a middle Miocene age. De Heinzelin & Glibert (1956) introduced the ‘Boldérien’ as a stratigraphic entity consisting of a basal gravel, a marine lower part and an upper continental part.

39The Bolderberg Formation was formally defined by De Meuter & Laga (1976) and re-iterated by Laga et al. (2001) as a succession of marine to continental deposits. The type locality is the village Bolderberg in the eastern Campine area. The Bolderberg Formation occurs furthermore in the subsoil of the central and eastern part of the Limburg province with outliers in the hills of the southern part of the Limburg province and the eastern part of the Flemish Brabant province (Deckers et al., 2019).

40The typical marine-continental cycle was originally used to subdivide the Cenozoic in the Belgian Basin (Rutot, 1883) and was also used in the former 1:40 000 mapping. Gullentops (1963, fig. 4) used the cycle as a sedimentary model for the Cenozoic in north Belgium. The basal Elsloo gravel consists of rounded pebbles and shark teeth, and is followed by dark green, glauconitic, slightly ligniferous, fossiliferous, medium fine-grained sand with a minor clay content. Micaceous intercalations are present. This lower part of the Bolderberg Formation passes gradually into a white, and rather coarse grained sand with lignite intercalations and glassy quartzite layers. De Meuter & Laga (1976) defined two members: the lower glauconite bearing Houthalen Member and the upper quartz-rich, pale yellow to white Genk Member. Within the Genk Member a very white silica sand occurs which was informally called Opgrimbie sand or Opgrimbie facies.

41A third member, the Opitter member, was proposed by Gullentops & Huyghebaert (1999) and mapped by Sels et al. (2001) on the geological map 18-10 Maaseik-Beverbeek. The proposal was based on the stratigraphic interpretation of an outcrop in the Opitter Molen sand pit by Gullentops (1963), and follows previous interpretations (a.o. de Heinzelin, 1963a). However, Houthuys & Matthijs (2020, this volume) and Dusar (archives BGD 048E0294) have argued that the Opitter sand, interpreted as part of the Bolderberg Formation in the sand pit, is erroneous. In a recently drilled well at Opitter (BGD 048E0294, DOV 48E0294), the stratigraphic sequence consisting of the Bolderberg, the Diest and the Kasterlee Formations can unequivocally be identified and is coherent with the regional stratigraphy at the southwestern side of the Neeroeteren Fault, thus rendering an additional fault superfluous.

42Based on only three samples, the Houthalen Member of the Bolderberg Formation has a modal grain size of 172 ± 12 µm, a clay content of 2.1 ± 0.7% and a D90 of 411 ± 274 µm (Verhaegen, 2020, this volume). One of those samples has a second coarse mode of 623 µm explaining also the large variation in D90. However, these three samples which are all from the Wijshagen borehole (BGD 048W0180, DOV kb18d48w-B181), should be reconsidered as representing the Genk Member rather than the Houthalen Member (Deckers & Louwye, 2019). Based on samples of the Opgrimbie quarry, Gullentops (1963, 1972-1973) reported a modal grain size of approximately 215 µm for the Opgrimbie facies. A sample from this facies in the Wijshagen borehole has a modal grain size of 296 µm, a clay content of only 0.7% and a D90 of 433 µm. Grain size data in Adriaens (2015) agree well with the data given above. The Genk Member has a similar smectite dominated clay mineralogy to the Houthalen Member and Berchem Formation, whereas the Opgrimbie facies has a different, kaolinite and illite-rich, clay mineralogy, probably due to a combination of a more southern source and intense leaching (Adriaens, 2015). The clay mineralogy indicates a coastal setting for the Genk Member and a fully continental setting for the Opgrimbie facies (Adriaens, 2015; Adriaens & Vandenberghe, 2020, this volume). In the Bolderberg Formation, highest glauconite values (below 20%) are recorded in the Houthalen Member, while the Genk Member contains no or only very limited amounts of glauconite. The non-glauconite fraction of all units is dominated by quartz. Bulk mineralogical data are available for the fraction <32 µm (Adriaens, 2015). The mineralogy (<32 µm) of the Houthalen Member is very similar to that of the Berchem Formation. However, the carbonate amount is very low (<1%) and consists only of siderite. The Genk Member is significantly less rich in clay minerals (<50%) and does not contain any glauconite minerals (Fe-rich clays). In contrast, the Genk Member does contain more secondary sulfate minerals and it has a larger amorphous content. The mineralogy of the Opgrimbie facies is similar to that of the Genk Member but without sulfates and with an increased kaolinite content. Compared to the Berchem Formation, a larger amount of Al₂SiO₅ polymorphs (kyanite, sillimanite and andalusite), staurolite and ultrastable minerals is recorded in the Bolderberg Formation. These differences from the Berchem Formation are apparent in the marine Houthalen Member but become even stronger in the continental Genk Member. The Berchem Formation is characterized by a large amount of epidote, amphiboles and garnet, making up on average more than 50% of the transparent heavy mineral composition (Verhaegen et al., 2019; Verhaegen, 2020, this volume). The difference between the two formations can be explained by the more southern location of the Bolderberg Formation, near the Roer Valley Graben, close to the input of sediments from the south through the Rhine-Meuse river system and local rivers draining the Ardennes and Brabant Massif (Verhaegen et al., 2019; Verhaegen, 2020, this volume).

43The lower boundary of the Bolderberg Formation with the Oligocene Voort or Eigenbilzen Formations is not easy to delineate on geophysical log data, but regularly coincides with an upwards increase in gamma ray values and decrease in resistivity values (Deckers et al., 2019) (Fig. 9). The lower part of the Bolderberg Formation consists of high gamma ray and relatively low resistivity values of the glauconite-rich, clayey, fine-grained Houthalen Member. The upper—generally thicker—part consists of low to very low gamma ray and relatively high resistivity values of the glauconite-poor, coarser-grained Genk Member. The transition between the Houthalen and Genk Members is consequently expressed by a gradual upward decrease in gamma ray values and increase in resistivity. This gradual change continues in the lower part of the Genk Member, and is interpreted as representing a coarsening upwards trend (Deckers & Louwye, 2017).

Figure 9. The Bolderberg Formation in the Wijshagen borehole and the correlations with the nearby Gruitrode borehole (according to Deckers & Louwye, 2017) and the Molenbeersel borehole (according to Deckers & Munsterman, 2020). The thickness of the Bolderberg Formation strongly increases from the Campine Block into the Ruhr Valley Graben as the Molenbeersel member proposed here is absent in the first and present in the latter. Dinoflagellate cyst analyses on the Wijshagen borehole were carried out by Louwye & Laga (2008). The lowermost sample was taken in the top of the Houthalen Member, which therefore—just like the lower part of the overlying Genk Member—belong to the Labyrinthodinium truncatum Zone. Note that between the Unipontedinium aquaeductum and the Amiculosphaera umbraculum Zones, the Achomosphaera andalousiensis and Gramocysta verricula are lacking in the Wijshagen borehole.

44Close to RVG border fault zone, the subdivision of the Bolderberg Formation in the Houthalen and Genk Members is still clearly expressed in the lithology of the Wijshagen borehole and in the geophysical logs of the Gruitrode borehole (BGD 048W0185, DOV kb18d48W-B186; Fig. 9). However, across this fault zone in the Molenbeersel borehole Deckers & Munsterman (2020, fig. 3) distinguished an additional 156 m slightly glauconitic and lignite-containing fine sand between the top of the Genk Sand and the base of the Diest Sand from which it differs by the marked increase in glauconite and therefore higher GR values in the latter. This additional 156 m thick interval has been a stumbling block in all previous interpretation attempts (see e.g. Demyttenaere & Laga, 1988; Verbeek et al., 2002; Broothaers et al., 2012). Deckers & Munsterman (2020) have argued that this additional interval is comparable to the Serravallian Vrijherenberg Sand in the Dutch stratigraphy. No comparable lithostratigraphic units of such age are known in Belgium and therefore a new lithostratigraphic unit has to be introduced. It is proposed to include this additional sand package in the Bolderberg Formation as the Molenbeersel member (see paragraph 2.3.5.).

45The Bolderberg Formation is topped by the basal gravel layer of the Diest Formation. On wireline logs, the boundary between the Bolderberg Formation and Diest Formation coincides with a subtle increase in gamma ray values caused by an increase in glauconite content (Deckers & Louwye, 2017).

2.3.2. Houthalen Member

46The well-developed, transgressive Elsloo gravel at the base of the Bolderberg Formation consists of reworked Oligocene components, dark blue, egg-shaped, indented phosphate pebbles and shark teeth (Vandenberghe et al., 1998). Tavernier (1954) already stressed the importance of the Elsloo gravel as a reference level. These characteristic pebbles occur under a thin glauconitic sand between Leuven and Tienen (Vandenberghe & Gullentops, 2001), while Houthuys (2014) reports similar pebbles in the Flemish Hill sand base gravel near Ronse. The Elsloo gravel is overlain by the marine Houthalen Member: a dark green, often clayey, medium fine-grained sandy unit, micaceous, slightly ligniferous and glauconitic. Similar to the Berchem Formation, dispersed and concentrated mollusks occur which are also reworked in the basal gravel of the superjacent Diest Formation (De Meuter & Laga, 1976). The Houthalen Member has a lower average glauconite content compared to the glauconitic sand of the Berchem Formation (17% versus >30%), which can be explained by a more landward position of the Bolderberg Formation with a stronger continental influence (Adriaens, 2015). The presence of lignite in the Houthalen Member furthermore testifies of a more proximal depositional setting, contrasting with the open marine depositional setting of the Berchem Formation (Deckers & Louwye, 2017).

47A first study with benthic foraminifera of the Houthalen Member led De Meuter (1970) to propose tentatively a lateral stratigraphical equivalence with the Antwerpen Member, and thus a middle Miocene age. De Meuter & Laga (1976) recognized both in the Edegem Member and the Houthalen Member the Trifarina gracilis rugulosa – Elphidium ungeri Zone and thus lowered the stratigraphic position to the lower Miocene. De Meuter (1980) finally proposed a position in between the Edegem and Antwerpen Members. Willems et al. (1988) stated that the Houthalen Member and the Edegem Member both hold the lower Miocene interregional benthic foraminifer B7 Zone of the IGCP 124 Working Group.

48Based on planktonic foraminifera, Hooyberghs & De Meuter (1972) attributed the Houthalen Member to the upper part of the N4 Zone and N5 Zone of Blow (1969) and a stratigraphic position between the Edegem Member and Antwerpen Member was inferred. Hooyberghs (1983) made a more detailed study of the planktonic foraminifera from the Houthalen Member and recognized tentatively the N5 and the N6 Zones of Blow (1969) of Burdigalian age. Hooyberghs & Moorkens (1988) confirmed the presence of the Burdigalian interregional NPF12 Zone (Spiegler et al., 1988) in the Houthalen Member (and in the lower part of the Antwerpen Member), while the Edegem Member holds the Aquitanian NPF11 Zone (cf. supra). In two sequence stratigraphic review papers, Vandenberghe et al. (1998, 2004) linked the Houthalen Member to the Edegem Member, a correlation that was not fully supported based on the recorded benthic and planktonic foraminifera which actually placed the Houthalen Member in between the Edegem and Antwerpen Member (see above). Martini & Müller (1973) found a similar nannoplankton assemblage in the Houthalen Member and the Edegem Member, a finding that was later corroborated by Verbeek et al. (1988) who stated that both members hold the nannoplankton NN2 Zone and NN3 Zone. Wouters (1978) recognized in the Houthalen Member the ostracod Pterygocytheris continens – Kuiperiana wanneri Zone, which is correlatable to the lower Miocene U2 zone of Gramann (1988).

49Louwye & Laga (2008) analyzed the dinoflagellate cysts a section in the Wijshagen core that was considered at that time to belong to the Houthalen Member. Their analyses showed that, following the biozonation of de Verteuil & Norris (1996), the entire analyzed section holds the DN4 and DN5 Zones and deposition took place some time during late Burdigalian and Langhian times. The calibrated biozonation by Dybkjær & Piasecki (2010) indicates the presence of the lower Langhian Labyrinthodinium truncatum and lower Langhian – lower Serravallian Unipontidinium aquaeductus Zones. Louwye & Laga (2008) suggested a major hiatus of circa 2 Ma between the Bolderberg Formation and the superjacent Diest Formation. More recently, based on a lithological re-analysis and correlation with the logged Gruitrode borehole, Deckers & Louwye (2017) re-interpreted the lithostratigraphy of the analyzed section of the Wijshagen borehole previously analyzed by Louwye & Laga (2008), and referred almost the entire section to the Genk Member (Figs 5, 8). Only the lowermost sample of the studied section was interpreted by Deckers & Louwye (2017) as belonging to the Houthalen Member. However, it has to be stressed that the boundary between the Houthalen and Genk Members in the Wijshagen borehole is not sharp but gradual. In any case, the age of the Houthalen Member has to be re-assessed. According to the dinoflagellate cyst biostratigraphy of Dybkjær & Piasecki (2010), the sole sample of the Houthalen Member in the Wijshagen borehole has an earliest Langhian age. The section of the Houthalen Member below the top sample remains unstudied for palynology and has an inferred pre-Langhian (or even Burdigalian) age (Fig. 6). This inferred pre-Langhian (Burdigalian) age for the Houthalen Member is thus in agreement with previous biostratigraphical studies with calcareous microfossils (cf. Hooyberghs & De Meuter, 1972; Martini & Müller, 1973; De Meuter & Laga, 1976; Wouters, 1978; Hooyberghs, 1983; Hooyberghs & Moorkens, 1988; Willems et al., 1988; see also Louwye & Laga, 2008). The Houthalen Member can be considered coeval with the Edegem and Kiel Members following the palynological analysis, and its topmost part possibly with the lowermost part of Antwerpen and Zonderschot Members.

2.3.3. Genk Member and Opgrimbie facies

50The Genk Member is the upper member of the Bolderberg Formation and consists of white to yellowish sand deposited in a more continental setting compared to the subjacent Houthalen Member. The continental influence is indicated by its quartz-rich nature, lack of significant glauconite, the presence of lignite and the heavy mineral and clay mineral composition (Gullentops, 1972-1973; Verhaegen, 2020, this volume; Adriaens & Vandenberghe, 2020, this volume). Macrofossils are generally lacking although shells are recorded at the lower part of the unit in the Wijshagen borehole (Deckers & Louwye, 2017). Based on the dinoflagellate cyst analysis in the Wijshagen borehole by Louwye & Laga (2008), correlated to chronostratigraphy using the zonation of Dybkjær & Piasecki (2010), the Genk Member in the eastern Campine area was deposited during the Langhian to earliest Serravallian, i.e. the same time interval as the main body of the Antwerpen Member in the Antwerp area (Fig. 6). The Zonderschot Member is a coeval unit lying geographically in between.

51The Genk Member has a yellowish color near the surface in the east Brabant area (Vandenberghe & Gullentops, 2001) and on the hill tops west of Brussels (‘Sables chamois’, see below) (Buffel & Matthijs, 2009). In the deeper subsurface it has a brownish-yellowish color (geological map 25 Hasselt), while in the eastern part of the same map the dominant color becomes white although some levels still have a yellowish color (Matthijs, 1999). Further eastwards, on the geological maps 26 Rekem and 18-10 Maaseik-Beverbeek the entire Genk Member is described as white sand and in this area also the very white silica glass quarried by the Sibelco company occurs.

52In the Sibelco sand pit in Opgrimbie a lignite complex of about 3 m thickness is observed within the Genk Member (Gullentops, 1963, 1972-1973). It undoubtedly corresponds to the prograding coastal peat swamps of either Morken Lignite Seam or the Frimmersdorf Lignite Seam which have the largest geographical distribution of the lower to middle Miocene Ville Formation lignites in the Lower Rhine Graben. The Morken Lignite Seam has a middle to late Burdigalian age and the Frimmerdorf Seam has a Langhian age (Utescher et al., 2012, fig. 3). In The Netherlands the Heksenberg Member of the Groote Heide Formation consisting of white quartz-rich sand is comprised in between these two seams (van Loon, 2009; van der Meulen et al., 2009; Deckers & Munsterman, 2020).

53Matthijs (1999) further subdivided the Genk Member in the eastern part of the geological map 25 Hasselt and established a fourfold subdivision based on the occurrence of gravel layers or equivalent levels of coarser grain size. The lowest unit has a gradual transition with the underlying marine glauconitic Houthalen Member. It is separated from the overlying sand by the Terlamen gravel, which corresponds to the lower gravel in the Bolderberg section and holds silicified mollusks concentrated from older reworked Bolderberg Formation sediments (de Heinzelin, 1963b). Above the Terlamen gravel occurs about a 10 to 15 m thick, medium-grained white sandy unit holding lignite. It is quarried as an industrial grade silica sand, the so-called Opgrimbie silver sand. The extreme maturity of the sand is partly caused by the combined effect of a deeply weathered provenance area (Gullentops, 1963, 1972-1973) and the leaching effect of humic acids from lignite (Gullentops, 1988; van Loon, 2009). Vandenberghe et al. (1998) and van Loon (2009) assumed a Burdigalian age for the onset of the swamp conditions leading to the formation of lignite in the Opgrimbie sand, and consequently associated this lignite with the Morken Lignite Seam rather than with the Frimmersdorf Lignite Seam of Langhian age. The quartzite in the Opgrimbie sand is compared to the Braunkohlen-Quartzit (Gullentops, 1963) or Nivelstein Sandstone (van Loon, 2009); it is considered as a silcrete cemented by originally abundant opal bioliths in the swamp vegetation (Gullentops, 1988), and a depositional model for the Opgrimbie sand is proposed by the latter author. Although this very white silica sand is not listed as a separate member in the stratigraphic inventories (see National Commission for Stratigraphy Belgium website, https://ncs.naturalsciences.be/paleogene-neogene/22-bolderberg-formation-bb) and neither in the legends of the 1:50 000 geological maps 26 Rekem and 18-10 Maaseik-Beverbeek, it is often regarded as a separate facies, mostly as Opgrimbie sand after the now abandoned Sibelco sand pit at this locality (Gulinck, 1961; Wouters & Vandenberghe, 1994; van Loon, 2009; Louwye et al., 2015). Other less common names for the Opgrimbie facies are Miocene glass-sand of Maasmechelen (Gullentops, 1972-1973), Maasmechelen Silver sand (Sels et al., 2001; Buffel et al., 2001) or ‘Mechelen aan de Maas sand’ (Laga, 1973). The exact lateral and vertical limits of this sand unit remain to be defined.

54The white Opgrimbie sand facies is topped by the Opgrimbie gravel (Matthijs, 1999) which is exposed in the former Sibelco sand pit (Gullentops 1963, 1972-1973, 1988). The Opgrimbie gravel consists of a few well-rounded blue flint pebbles and is somewhat undulating. It is the only gravel level continuous enough to be mapped on the geological map 26 Rekem (Buffel et al., 2001). On the geological maps 26 Rekem and 18-10 Maaseik-Beverbeek the Opgrimbie gravel subdivides the Genk Member in two parts, BbGe a&b. The grain size and heavy mineral composition data of both units exposed in the Sibelco sand pit at Opgrimbie are discussed by Gullentops (1963, 1972-1973). In boreholes of the geological map 25 Hasselt, an upper third gravel layer could be identified and was called the Meulenberg gravel (Matthijs, 1999). The sandy unit between the Opgrimbie and Meulenberg gravel beds is 6 to 7 m thick, contains some glauconite pellets and displays cross bedding structures. The base of the latter sand is exposed above the Opgrimbie gravel in the former Sibelco sand pit (Gullentops, 1963, 1972-1973, 1988). The sand above and below the Meulenberg gravel is lithologically very similar. Gulinck (1961) reports several levels of bluish flint pebbles occurring in the As area (geological map 26 Rekem) occurring about 10 to 15 m above the lignite zone in the white Opgrimbie sand below the Opgrimbie gravel, and about 60 m above the Elsloo Gravel at the base of the Bolderberg Formation.

55Vandenberghe et al. (1998, 2004) proposed three stratigraphic sequences in the Bolderberg Formation mainly based on the section in the Sibelco sand pit and correlates the three sequences with the threefold division of the Berchem Formation. Deckers & Munsterman (2020) correlated the main (lower to middle Langhian) coarsening upwards body of the Genk Member to the upper part of the sequence D of Rasmussen (2004a, b). The uppermost (upper Langhian) part of the Genk Member was correlated with the lower part of sequence E of Rasmussen (2004a, b). Although the criteria for sequence recognition remain unchanged, new detailed controls on the stratigraphic ages of the deposits, and also the refinement of the global sequence recognition in Hardenbol et al. (1998), compared to Haq et al. (1987), are required for a re-evaluation of the present sequence interpretations.

2.3.4. The lower and middle Miocene in the Maaseik borehole

56The Maaseik cored borehole (BGD 49W0220, DOV kb18d49w-B220, Fig. 1) was drilled in the easternmost part of the Campine area near the border with The Netherlands and is structurally located on the shoulder of the Roer Valley Graben. Vandenberghe et al. (2005) reported on the Miocene, Pliocene and Quaternary deposits through a holostratigraphical multi-proxy analysis. The Miocene Breda Formation was encountered between a depth of 302 m and 198 m. The base of the Breda Formation was not attained during the drilling and the formation is overlain by the upper Miocene unit X (Fig. 10) (Vandenberghe et al., 2020; Louwye & Vandenberghe, 2020, this volume). A biostratigraphical analysis with marine palynomorphs (mainly dinoflagellate cysts) was carried out following the biozonation by de Verteuil & Norris (1996), defined in the eastern Coastal Plain of the US. The lowermost part of the sequence (samples 295.8 m and 292.4 m) was tentatively attributed to the upper Langhian–lower Serravallian DN5 Zone. The above lying sequence holds the Zones DN6 to DN9 implying a correlation with the mid-Serravallian to upper Tortonian.

Figure 10. Lithostratigraphy, biostratigraphy, chronostratigraphy and geophysical logs of the Maaseik borehole, modified after Vandenberghe et al. (2005). Vertical dotted line: uncertain range, horizontal solid lines: correlation from lithological and geophysical boundaries as identified by Vandenberghe et al. (2005, figs 2 & 7). Note the small, black squares on the horizontal lines marking the correlation between lithology-geophysical log signatures and biozone boundaries. Dinoflagellate cyst zonation after Dybkjær & Piasecki (2010). Bolboforma zonation after King (2016). The interval ‘unknown facies in Campine’ correlates with the upper part of the Molenbeersel member (see text 2.3.5.).

57The Breda Formation is now re-interpreted following the biozonation of Dybkjær & Piasecki (2010) for correlation purposes with the dinoflagellate zonation of the Berchem Formation and the Bolderberg Formation discussed above. The lowermost part (samples 295.8 m to 279.9 m) hold the Labyrinthodinium truncatum/Unipontedinium aquaductus Zones (Fig. 10). No further differentiation could be made since the key species U. aquaeductus was not recorded. This section of the core has an inferred Langhian to early Serravallian age. The above lying Achomosphaera andalousiensis Zone is recognized in the interval holding the three samples (275.8 m, 270.9 m and 265.8 m) based on the presence of the eponymous species together with Cannosphaeropsis passio and Cerebrocysta poulsenii. Both latter species have their last occurrence in this zone according to Dybkjær & Piasecki (2010). The A. andalousiensis Zone has an early to mid-Serravallian age. The Gramocysta verricula Zone is recognized in the above lying section (samples 256.3 m and 245.5 m). The zone has an inferred Serravallian to early Tortonian age. The above lying section until the upper boundary holds the Tortonian Amiculosphaera umbraculum Zone (samples 234.5 m and 227.5 m) and the upper Tortonian Hystrichosphaeropsis obscura Zone (samples 220.5 m to 191.5 m). The superjacent unit X holds also the H. obscura Zone (Louwye & Vandenberghe, 2020, this volume).

58The precise boundaries between the dinoflagellate zones as indicated on Figure 10 are determined by the investigated sample depths combined with the lithological information from the core descriptions and the geophysical log signatures. The latter lithological changes and log signatures fit well with the dinoflagellate cyst zone divisions. Vandenberghe et al. (2005) already stipulated that in the Maaseik well a lithofacies unknown in Campine area is present (‘unknown facies in Campine’, Fig. 10). This interval in the Maaseik core corresponds partly to the A. andalousiensis Zone and entirely to the G. verricula Zone. The latter zone is indeed absent in the Antwerp area and Campine area where the youngest recognized zone is the A. andalousiensis Zone. Vandenberghe et al. (2005) furthermore labelled in the Maaseik core a section as “Upper Antwerp Sand” (Fig. 10) which now, after the biostratigraphic re-interpretation following Dybkjær & Piasecki (2010) corresponds to the lower part of the A. andalousiensis Zone. The deposits in the Maaseik core holding the upper part of the A. andalousiensis Zone and the Gramocysta verricula Zone correspond thus to the minimal duration of the hiatus observed in the Antwerp and Campine areas (see above).

59The Bolboforma of the Breda Formation were analyzed by Hooyberghs et al. (2004) and four biozones were recognized. The revision of the Bolboforma biozones by King (2016) is used here. From top to base following Bolboforma biozones were recognized: the Bolboforma metzmacheri Zone (201.5 m to 227.5 m; 9.54 Ma to 8.78 Ma), the Bolboforma capsula Zone (sample 228.5 m; 10.5 Ma to 9.54 Ma), a barren interval (sample 234.5 m), the Bolboforma compressispinosa Zone (samples 237.5 m and 246.5 m; 11.9 Ma – 11.56 Ma), the Bolboforma badenensis Zone (sample 259.5 m; 12.6 Ma to 11.9 Ma). The Bolboforma subfragoris zone (11.56 Ma – 10.50 Ma) was not recognized between the B. compressispinosa and B. capsula zones, most probably because of the barren interval of circa 10 m. If the barren interval would not correspond to the missing B. subragoris zone but on the other hand to either the B. capsula or B. compressispinosa zone, a hiatus of about 1 Ma could be present at that level. The Bolboforma zonation and stratigraphic interpretation confirms the dinoflagellate cyst interpretation notwithstanding minor inherent discrepancies related to calibration.

2.3.5. Molenbeersel member

60The additional sand interval between 369 m and 525 m in the Molenbeersel borehole (see section 2.3.1.) is here proposed as the new Molenbeersel member. Compared to the underlying Genk Member the unit is characterized by a markedly higher GR signal (Fig. 9). This is consistent with its lithology of brown-gray to gray-green, clay- and shell-bearing silt and fine-grained sand that contains lignite and glauconite, in contrast to the quartz-rich Genk Sand. The gamma ray values in the Molenbeersel member interval increase from a basal gravel towards a maximum in the central part, which is richest in glauconite and shells (including Glycymeris) and is also micaceous. From this maximum, a decrease takes place in the gamma ray values towards the top section, which coincides with an increase in lignite. The top of the Molenbeersel member in the Molenbeersel borehole is capped by the basal gravel layer of the Diest Formation as is the case with the Genk Member in the Campine area (Fig. 9). On wireline logs, this boundary between the Bolderberg Formation and Diest Formation coincides with a subtle increase in gamma ray values caused by an increase in glauconite-content (Deckers & Louwye, 2017). Unfortunately, no relevant biostratigraphic data are available in the Molenbeersel borehole itself for direct comparison with the nearby Dutch RVG stratigraphy or with the nearby Maaseik borehole in the Belgian RVG. Comparison with the Vrijherenberg Sand, as discussed in Deckers & Munsterman (2020) in the borehole Groote Heide, is mainly based on the trends in the GR signal between the Genk Sand and the Diest Sand. The Vrijherenberg Sand has a Serravallian age based on dinoflagellate cysts biostratigraphy. The implied Serravallian age of the additional Molenbeersel member interval is compatible with the age interval of the dinoflagellate cyst hiatus between the Genk Sand and the Diest Sand in the nearby Wijshagen borehole in which the Molenbeersel member is missing (Fig. 9; Deckers & Munsterman, 2020, fig. 3).

61In the nearby Maaseik borehole the base of the upper Miocene is interpreted at circa 240 m depth (see 2.3.4.). The Diest Formation nature of this glauconitic sand is confirmed above 235 m by their calcareous microfossils content resembling the Deurne and Dessel Members of the Berchem Formation. Underlying the upper Miocene occurs fine (modal size 175–200 µm) and slightly glauconitic (2–7%) sand, herein interpreted as belonging to the upper part of the Molenbeersel member, which contains in the upper part the Serravallian dinocyst zones A. andalousiensis and G. verricula of Dybkjaer & Piasecki (2010) (Fig. 10). Part of the A. andalousiensis zone in the Maaseik core was also recognized in the Antwerpen Member of the type area (Figs 6, 8). It is therefore reasonable to correlate indirectly the Molenbeersel member with part of the A. andalousiensis and/or the Gramocysta verrricula Zones, i.e. the part of the core that was interpreted as “unknown facies in the Campine area” by Vandenberghe et al. (2005). A Serravallian age could be postulated for the Molenbeersel member.

2.3.6. Heizel member or ‘Sables chamois’

62Le Hon (1862) introduced the name ‘Sables chamois’ to describe an isolated sandy unit on the top of the hills west of Brussels (Fig. 1). The stratigraphical position of these ‘Sables chamois’ remained debated for many decades until Leriche (1934), based on the presence of shark teeth in the base of the deposit, proposed a correlation with the upper Miocene deposits of northern Belgium. The ‘Sables chamois’ were subsequently described in detail by Gulinck (1956), and de Heinzelin (1956) suggested a correlation of the ‘Sables chamois’ with the lignite holding Bolderberg Formation although without providing an argumentation. The ‘Sables chamois’ were formally re-described by De Meuter & Laga (1976) as a yellow-brown, fine-grained sand without fossils, and they proposed informally the name Heizel sand for the unit. A gravel bed consisting of flint pebbles, shark teeth, marine mammal bone fragments, and plant fragments, already described by Leriche (1934) and Gulinck (1956), is present at the base of the unit. De Heinzelin (1963c) correlated the gravel bed at the base of the ‘Sables chamois’ with the Elsloo gravel at the base of the Bolderberg Formation. The gravel bed was called the Heizel gravel (Tavernier & de Heinzelin, 1963; De Meuter & Laga, 1976). Neither absolute nor relative biostratigraphical datings are until now available for the ‘Sables chamois’.

3. Depositional environment and geographical distribution

3.1. Depositional environment of the Berchem and Bolderberg Formations

63The abundance of shallow marine and inner neritic dinoflagellate cyst taxa in the Berchem Formation in the type area indicates deposition in a shallow marine environment (Louwye et al., 2000) and corroborate similar observations by Doppert et al. (1979) based on benthic foraminifera. However, the presence of oceanic dinoflagellate cyst taxa in the Antwerpen Member also testifies of a sporadic oceanic influence through currents in the shallow depositional environment of the southern North Sea Basin, most probably during periods of high sea level. The presence of abundant authigenic glauconite in the Antwerpen Member is indicative of slow sedimentation rates generally associated with a marine transgression and a depositional water depth deeper than 15 to 20 m (McRae, 1972; Giresse & Odin, 1973).

64Based on teleost otoliths, Huyghebaert & Nolf (1979) suggested deposition of the Zonderschot Member in a warm and rather calm, littoral to neritic environment, and consider it as shallower than the depositional environment of the Antwerpen Member. This is supported by the bivalves from the Zonderschot Member indicating a similar depositional near shore environment below wave base, most probably in an embayment (Ringelé, 1974). The presence of dinoflagellate cyst species with an oceanic to outer neritic affinity in the other mainly marginal marine dinoflagellate cyst assemblage of the Zonderschot Member at the southernmost rim of the depositional area of the Berchem Formation may represent a maximum flooding surface at the basin margin (Louwye, 2000).

65The Genk Member of the Bolderberg Formation was deposited in a marginal marine depositional environment (Louwye & Laga, 2008; Deckers & Louwye, 2017) with limited short-lived incursions of enhanced continental and fluviatile input, as testified by the variations in marine organic-walled palynomorphs (dinoflagellate cysts, acritarchs), organic-walled non-marine and terrestrial palynomorphs (green algae, pollen), and the presence of lignite and wood fragments. A more proximal depositional setting than the more open marine depositional environment of the coeval Berchem Formation in the Antwerp area can be postulated (Deckers & Louwye, 2017). The well-rounded and very well sorted grains point to a beach environment also suggested by the presence of gravel layers (see also van Loon, 2009). Some rare cross beds also point to a higher energy environment. The relative shallow depositional environment of the Genk Member despite the deposition during a eustatic sea-level rise related to the middle Miocene Climatic Optimum (MMCO, 17–14.5 Ma) (Zachos et al., 2001; Miller et al., 2005;), can be explained by an increase in sediment supply (Deckers & Munsterman, 2020). A similar explanation was given for the synchronous (Langhian) shallowing in the eastern North Sea Basin (Rasmussen et al., 2010).

66As mentioned above, the Zonderschot Member of the Berchem Formation probably occupies a geographically transitional position between the open marine and the marginal marine environments of the Antwerpen Member of the Berchem Formation and the Genk Member of the Bolderberg Formation, respectively.

67The end of the MMCO marks the start of a eustatic sea-level fall (Zachos et al., 2001; Miller et al., 2005), and coincides with the transition from the Genk Member towards the—hereby newly introduced—Molenbeersel member of the Bolderberg Formation (Deckers & Munsterman, 2020). The lithology of the Molenbeersel member, however, does not reflect a shallowing after the Genk Member, but on the contrary, a deepening of the depositional environment, with a return of glauconite (higher gamma ray values) and reduction of the lignite content (Fig. 9). The high gamma ray values in the central part of the Molenbeersel member probably reflect maximum flooding. This maximum flooding surface was indeed correlated by Deckers & Munsterman (2020) with an interval in the Groote Heide borehole where a maximum of open marine dinocysts species was noted by Munsterman et al. (2019). The latter authors’ dinocysts species analyses indicated a middle to early late Serravallian age for the maximum flooding surface. Also, in other parts of the North Sea Basin, such as the southern Roer Valley Graben or eastern North Sea Basin, indications for Serravallian transgression were found despite eustatic sea-level lowering (Rasmussen et al., 2010; Rasmussen & Dybkjær, 2014; Thöle et al., 2014; Prinz et al., 2017). Rasmussen (2004a) explained the relative sea-level rise during eustatic sea-level lowering by Serravallian tectonic subsidence of the North Sea Basin. Alternatively, Deckers & Munsterman (2020) proposed that a strong reduction of the input of sediments after the Langhian—under continued subsidence—might also explain the relative sea-level rise in the Serravallian.

68The reduction in gamma ray values and increase in lignite content in the upper part of the Molenbeersel member indicates a shallowing of the depositional environment. It was probably during this shallowing that former—relatively condensed—deposits of the Molenbeersel member on top of the Campine area were eroded, as reflected by the Serravallian hiatus in the Wijshagen borehole (Deckers & Munsterman, 2020; Fig. 9). During the Tortonian, the Berchem and Bolderberg Formations were transgressed and covered by the Diest Formation.

3.2. Geographical distribution

69The early – middle Miocene strata encountered in the subsurface of northeastern Belgium generally dip in a northern direction. The glauconitic sand of the Berchem Formation outcrops in the city of Antwerp and is buried up to more than 100 m further north at the boundary with The Netherlands. As a result of differential subsidence of the Roer Valley Graben, the depth also increases in an easterly direction. Within the Roer Valley Graben itself, the base of the Bolderberg Formation is situated at its maximum depth of 680 m (Fig. 9; Broothaers et al., 2012). In their southernmost occurrences, the early to middle Miocene strata are only preserved on hill tops, up to an elevation of over +50 m reference level. The Heizel sand or ‘Sables chamois’ were correlated with the Bolderberg Formation (see above) and occurs on hill tops in the Brussels area (Fig. 1), while further to the east the Houthalen Member of the Bolderberg Formation was observed on the Pellenberg hill near Leuven. Other relicts are found on hilltops in southern Limburg and are locally only preserved as sandstone boulders (Creemers & Dreesen, 2017; Fig. 1). The sand of the Opgrimbie facies subcrops and is quarried close to the Meuse river. The bluish egg-shaped pebbles at the base of the Flemish Hills formation on hilltops in northwestern Belgium are rather similar to those reported at the base of the Houthalen Member, and are suggestive of a Miocene age (Adriaens, 2015).

70A strong northern heavy mineral signature characterizes glauconite-rich sand of the Berchem Formation. This signal was mixed with continental signatures in the southeastern part of the Campine area as testified by the reduced amount of glauconite, the presence of lignite in the Bolderberg Formation, especially in the Genk Member, and by the more southern continental heavy mineral signature. Seismic interpretations show that the clastics of the Genk Member were deposited as part of a northwest prograding delta-system (Deckers, 2015). According to Verhaegen (2019) the main source of sediments from the south was the weathered sedimentary cover of the Brabant Massif and Ardennes, drained by local rivers and the larger Meuse river. Further landward in the subsiding Roer Valley Graben, thick lignite seams of the Ville Formation formed in Germany (Schäfer et al., 2005). Seaward of this delta-system, the glauconitic sand of the Antwerpen Member was deposited under low sedimentation rates, indicative for sediment starvation (Deckers & Louwye, 2019). Consequently, the boundary between the Genk and Antwerpen Members marks the maximum extent of the Langhian delta-system. In the new 3D geological model of Flanders (the G3Dv3-model) (Deckers et al., 2019), this boundary was estimated to have been situated roughly at the region where the Diest Formation strongly incised in the underlying units. This gully incision at the base of the Diest Formation was thought to be the result of early Tortonian marine ingression with strong (tidal) current erosion into latest Serravallian fluvial channels (Vandenberghe et al., 2014; Houthuys et al., 2020, this volume). Because of their relatively elevated position, the topsets of the Langhian clinoforms of the Genk Member probably formed a barrier against the Tortonian tidal currents that therefore formed the gully incisions only in their toeset region (see fig. 7 in Houthuys, 2014). The Langhian clinoforms may thereby also have redirected these Tortonian currents into the Hageland bay where maximum erosion took place.

71Contrary to the relatively high-lying Campine area, the differentially subsiding Roer Valley Graben was thought not to have been influenced by the abovementioned erosive processes. Therefore, it is expected to contain the most complete Miocene succession. In the Molenbeersel borehole (Fig. 9), located in the center of the RVG near the transitional area between the Berchem and Bolderberg Formations, the upper boundary of the Genk Member is situated at a depth of ca. 520 m overlain by glauconitic, lignite-poor, shelly sand. The lithology of this sand is not characteristic for the Diest Formation, and in the nearby Maaseik borehole, age-equivalent strata to the Diest Formation occur at a much shallower depth according to Vandenberghe et al. (2005; base at circa 240 m depth). Demyttenaere & Laga (1988) interpreted this sand as belonging to the Berchem Formation. However, compared to the Berchem Formation, the sand in the Molenbeersel borehole is much paler and contains less glauconite and some lignite. More recently, Deckers & Munsterman (2020) correlated this sand with the early to latest Serravallian stratigraphic succession in the Groote Heide borehole located in the southeastern part of The Netherlands. They interpreted this sand as belonging to the Dutch Vrijherenberg Sands, equivalent to the German Neurath Sands, located on top of the main lignite seams. In this study, this sand interval in the Molenbeersel borehole is introduced as the Molenbeersel member. In the Campine area, the Molenbeersel member was not yet described, probably due to non-deposition or—more likely—erosion below the base of the Diest Formation. A thin veneer of early to mid-Serravallian deposits in the Campine area was recorded only in the Kalmthout and Retie wells as belonging to the Berchem Formation (Fig. 8).

72Whereas the Genk Member of the Bolderberg Formation has a different lithology than the Berchem Formation, distinguishing the Houthalen Member of the Bolderberg Formation from the Berchem Formation is more difficult. Although the lithology of the Houthalen Member and Zonderschot Member is very similar, i.e. shell-rich, dark green, clayey, glauconite-rich, micaceous fine sand with lignite, these units are thus not entirely coeval (see above) and therefore the Zonderschot Member cannot be regarded wholly as a lateral facies of the Houthalen Member. However, in the Pellenberg Hill near Leuven the characteristic Elsloo gravel was observed together with glauconitic sand and was interpreted by Verhaegen (2019) as the Houthalen Member. The heavy mineral composition of this glauconitic sand has a higher proportion of metamorphic minerals and a lower proportion of epidote, amphibole and garnet compared to the Berchem Formation, making it feasible that it belongs to the more continentally influenced Bolderberg Formation (Verhaegen, 2020, this volume). This observation would place the boundary between the Houthalen Member and the Antwerpen Member in the area where the lower to middle Miocene sediments were eroded by the Diest gully.

73In the G3Dv3-model, the lower Burdigalian Edegem Member of the Berchem Formation was mapped in the area surrounding Antwerp city, from Heist-op-den-Berg in the southeast towards Brasschaat in the northwest (Deckers et al., 2019). The presence of the Edegem Member further northwest in the Harbor of Antwerp remains uncertain. In the Kalmthout borehole, coeval deposits of the Edegem Member are recorded (see 2.2.). Dinoflagellate cyst biostratigraphy indicates that in the Campine area the mid-Burdigalian to lower Serravallian deposits, i.e. deposits coeval with the Kiel and Antwerpen Members in the type area, are all lithologically regarded as Antwerpen Member, according to the borehole logs of the Geological Survey of Belgium in the absence of sediment analyses of the lithologically not much differing members. Unpublished biostratigraphical analysis of benthic foraminifera (archives Geological Survey of Belgium) in boreholes Rijkevorsel and Poederlee corroborate the dinoflagellate cyst analysis.

4. Conclusion - proposals for stratigraphic re-evaluation and emendations

4.1. The status of the Kiel Member

74The Kiel and the Antwerpen Members were formally defined by De Meuter & Laga (1976) and described in detailed lithologs by De Meuter et al. (1976). According to these authors both members are lithologically rather similar and the difference lies mainly in the absence or presence of calcareous fossils, respectively, and grain-size difference; the sand of the Kiel Member is regarded as a medium fine-grained to coarse-grained sand while the Antwerpen Member sand is medium fine-grained. Furthermore, De Meuter & Laga (1976) state that the Kiel Member is non-fossiliferous in the southern part of the Antwerp area where the unit can readily be recognized, while more to the north and east the Kiel Member becomes fossiliferous and indistinguishable from the superjacent Antwerpen Member. Still, De Meuter et al. (1976) noted that the Kiel Member occasionally holds friable shell fragments in the southern part of the Antwerp area.

75Everaert et al. (2019; 2020, this volume) and De Schutter & Everaert (2020, this volume) recently reported in detail on several temporary outcrops of the Kiel Member in Antwerp. Lithostratigraphically, they identify the Kiel Member with respect to the overlying Antwerpen Member by a slightly paler color of the Kiel Member due to its lower glauconite and clay fraction content and its coarser-sized sand fraction. They could document a well-preserved fauna and even correlate sections by specific mollusk levels. This correlation showed that the boundary between the Kiel and the Antwerpen Members has the geometry of an angular unconformity by the northwards disappearing of the DN3 Zone, i.e. the top part of the Kiel Member. Their data confirm that the Kiel Member, decalcified in the south, becomes fossiliferous northwards. At the time, such detailed analysis was unknown to De Meuter et al. (1976) which explains why these authors interpreted the entire fossiliferous temporary outcrop Kievitstraat, located north of the Kiel type area, as the Antwerpen Member noting however a layer of sandstone pebbles within the sequence. A biostratigraphical analysis with dinoflagellate cysts showed that the sediments above this pebble layer belong to the Langhian Labyrinthodinium truncatum Zone and are correlatable with other sections of the Antwerpen Member in the vicinity. However, the deposits below the pebble layer belong to the mid-Burdigalian Exochosphaeridium insigne Zone (Louwye et al., 2000) and are therefore correlatable to sections of the Kiel Member more to the south. Consequently, the late Burdigalian Cousteaudinium aubryae Zone is lacking in the Kievitstraat outcrop which implies a local considerable hiatus at this site of circa 1.8 Ma. With the present knowledge as documented above, the mid-Burdigalian sediments below the sandstone pebble layer should have been interpreted as belonging to the Kiel Member, albeit fossiliferous.

76In summary, the Kiel Member is in its type area, south of the city of Antwerp, decalcified and only holds ghosts or fragile fragments of mollusks and, moreover, holds a poorly preserved dinoflagellate cyst assemblage. The taphonomic processes can be attributed to postdepositional alteration phenomena such as decalcification in combination with (mild) oxidation.

77This present geometric and stratigraphic model for the relation between Kiel and Antwerpen Members needs further sedimentological, mineralogical and stratigraphical support to fully understand its evolution and determine its extension north of the city of Antwerp into the Campine.

4.2. A new member of the Bolderberg Formation: the Molenbeersel member

78A glauconite- and lignite-bearing middle Miocene sandy unit with a thickness of 156 m is recorded in the Molenbeersel borehole between the Genk Member of the Bolderberg Formation and the Diest Formation (Fig. 9) (Deckers & Munsterman, 2020). The Molenbeersel well is located in the strongest subsiding area of the Roer Valley Graben. The latter authors informally interpreted this sand as part the Dutch Vrijherenberg Sands and considered them equivalent to the German Neurath Sands. Here we propose this unit as a new lithostratigraphic unit, the Molenbeersel member, within the Bolderberg Formation (Fig. 9).

79The Molenbeersel member consists of brown-gray to gray-green, clay- and shell-bearing silt and fine-grained sand, containing lignite and glauconite. The central part contains the most glauconite and shells (including Glycymeris) and is also micaceous. More lignite is present towards the top. The unit is bounded by gravel at the base and top.

80The member is named after the hamlet Molenbeersel, located near the town of Kinrooi, in the province of Limburg, northeasternmost Belgium. The type section is the Molenbeersel well, DOV-code: kb18d49w-B225 and BGD-code: 049w0225 (X-coordinate: 247691.5; Y-coordinate: 207743.3; Z: 33 m); interval 525–369; thickness: 156 m along hole. The member is present in the Roer Valley Graben (borehole Molenbeersel) and Venlo Block (borehole Groote Heide), and absent to the west in the Wijshagen borehole on top of the Campine Block. The basal Molenbeersel member is marked by a sharp increase in gamma ray values compared to the underlying Genk Member, reaching a maximum in the middle part of the unit (Fig. 9). The relatively high gamma ray values in the central part are probably caused by higher clay and glauconite contents. Near the top of the member, the gamma ray values are very low again. The boundary with the overlying Diest Formation coincides with a modest increase.

81The presence of shells, glauconite and open marine dinoflagellate cysts indicates a shallow marine depositional environment. The highest glauconite content and number of open marine dinoflagellate cysts is recorded in the middle part of the member (coincident with the highest gamma ray values), interpreted as a maximum flooding surface by Deckers & Munsterman (2020). The presence of lignite and coastal palynomorphs indicate a near coastal depositional environment.

82The Molenbeersel member occurs in between the underlying Genk Member of the Bolderberg Formation and the superjacent Diest Formation. This is similar to the geometric position of the Vrijherenberg Sand in the Groote Heide borehole located in the Dutch RVG. In addition, the GR evolution in the Molenbeersel member is similar to its evolution in the Vrijherenberg Sand. The Vrijherenberg Sand contains dinoflagellate cyst zones (sensu Munsterman et al., 2019) practically spanning the full range of the Serravallian time (Deckers & Munsterman, 2020). In the nearby Maaseik borehole in the Belgian RVG the upper Miocene is immediately underlain by sand, interpreted as belonging to the uppermost part of the Molenbeersel member, of Serravallian age based on dinoflagellate cyst biostratigraphy. This makes a case for the mid-Serravallian age of the top of the Molenbeersel member. Also, more biostratigraphical and comparative sedimentological data on the Molenbeersel member are needed.

5. Acknowledgements

83Johan Matthijs (VITO) and Isaac Berwouts (Sibelco) are thanked for information and discussion on the Opgrimbie facies and the Genk Member. Karen Dybkjær (GEUS) and Robert Speijer (KU Leuven) are thanked for their constructive reviews.

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