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Thirty Devonian-Carboniferous Boundary sections of the Rhenish Slate Mountains and adjacent subsurface areas are reviewed with respect to litho-, event, conodont, ammonoid, sequence, and chemostratigraphy. In the interval from the base of the uppermost Famennian (Wocklum Beds, Wocklumian) to the base of the middle Tournaisian (base Lower Alum Shale), 11 conodont and 16 ammonoid (sub)zones are distinguished. The terminology of the Hangenberg Crisis Interval is refined, with an overall regressive Crisis Prelude below the main Hangenberg Extinction, which defines the base of the transgressive Lower Crisis Interval (Hangenberg Black Shale). The glacigenic and regressive Middle Crisis Interval (Hangenberg Shale/Sandstone) is followed by the overall transgressive Upper Crisis Interval that can be subdivided into three parts (I to III) with the help of conodont stratigraphy (upper  costatus-kockeli  Interregnum = upper  ck I,  Protognathodus kockeli  Zone, and lower part of  Siphonodella  ( Eosiphonodella )  sulcata  s.l./ Pr. kuehni  Zone).  Protognathodus kockeli  includes currently a wide range of forms, which variabilities and precise ranges need to be established before a precise GSSP level should be selected. Returning to its original definition, the former Upper  duplicata  Zone is re-named as  Siphonodella  ( S. )  mehli  Zone. It replaces the  S.  ( S. )  jii  Zone, which is hampered by taxonomic complications. The  S.  ( S. )  quadruplicata  Zone of Ji (1985) is hardly supported by Rhenish data. The entry of typical  S.  ( S. )  lobata  (M1) characterises an upper subdivision (subzone) of the  S.  ( S. )  sandbergi  Zone; the new  S.  ( S. )  lobata  M2 enters much earlier within the  S.  ( S .)  mehli  Zone. The ammonoid-defined base of the Wocklum-Stufe (Upper Devonian = UD VI) begins with the  Linguaclymenia similis  Zone (UD VI-A 1 ). The oldest  S.  ( Eosiphonodella ) enter within the  Muessenbiaergia bisulcata  Zone (UD VI-A 2 ). The traditional  Parawocklumeria paradoxa  Zone of Schindewolf (1937) is divided into successive  P. paprothae  (VI-C 1 ),  P. paradoxa  (VI-C 2 ), and  Mayneoceras nucleus  (VI-C 3 ) Subzones. In the lower Tournaisian (Lower Carboniferous = LC I), the  Gattendorfia subinvoluta  Zone is subdivided into  G. subinvoluta  (LC I-A 2 ) and “ Eocanites ”  nodosus  (LC I-A 3 ) Subzones. The  Paprothites dorsoplanus  Zone (LC I-B) can be divided into  Pap. dorsoplanus  (LC I-B 1 ) and  Paragattendorfia sphaeroides  (LC I-B 2 ) Subzones. Potential subdivisions of the  Pseudarietites westfalicus  (LC I-C) and  Parag. patens  Zones (LC I-D) are less distinctive. The unfossiliferous or argillaceous upper part of the Hangenberg Limestone and the overlying Lower Alum Shale Event Interval remain regionally unzoned for ammonoids.

Review of Devonian-Carboniferous Boundary sections in the Rhenish Slate Mountains (Germany)