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International Journal of Paleobiology & Paleontology Research Article 10 min read

Planktic Foraminiferal Biostratigraphy of the Cretaceous Oceanic Red Beds in Gyangze, Tibet

Yuewei L, Chengshan W, Guobiao L*, Jinbiao Z, Jingjing W and Kezhantu B
* Corresponding author
ISSN: 2642-1283  10.23880/ijpbp-16000127  Received: November 12, 2021  Published: December 01, 2021
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Keywords
CORB Chuangde Formation Planktonic Foraminifera Late Cretaceous Gyangze Tibet
Abstract

A set of CORBs developed in the Northern Tethys Himalayan Subzone, southern Tibet, China. The CORB, which is called as the Chuangde Formation, in Gyangze area is mainly composed of micofossil-bearing red limestone and shale intercalated with siliceous rock (chert). This study focuses on the planktic foraminiferal biostratigraphy of the CORB in Gyangze area, Southern Tibet, China. the important elements of the planktic foraminiferal assemblage include Archaeoglobigerina bowi, Globigerilloides ultramicra, G.prairiehillensis, Globotruncana linneiana, G. lapparenti, G. arca, G.ventricosa, G. falsostuarti, Globotruncanella havanensis, Globotruncanita elevata, G. stuartiformis, G. stuarti, Hedbergella holmdelensis, Heterohelix globulosa, H. striata, Radotruncana calcarata, R. subspinosa, and Rugoglobigerina rugosa etc. Four planktonic foraminiferal biozones were recognized (in ascending order) G. elevata, G. ventricosa, R. calcarata and G. havanensis zones, which provided the Chuangde Formation (CORB) with an age of Late Cretaceous Campanian.

Introduction

Oceanic/marine red beds are widely distributed in the global oceans during the entire Phanerozoic period, usually after oceanic anoxic events. They represent a typical oxygen- rich sedimentary environment and play a important role in marine scientific research. Marine red beds of Cretaceous age, also termed the Cretaceous oceanic red beds (CORBs) have been reported from various palaeogeographical settings and in different time intervals worldwide, which usually comprise reddish to pinkish to brownish sedimentary rocks deposited in pelagic-hemipelagic marine environments and generally comprised of limestone, marl, shale, and/or chert, span the Aptian-Maastrichtian interval of Late Cretaceous, and have been reported worldwide [1, 2, 3, 4, 5, 6, 7, 8, 9]. Cretaceous Oceanic Red Bed (CORB) deposition is of great significance to paleoceanography evolution and is one of the most attractive topics in Cretaceous research in the world.

A set of CORBs developed in the Northern Tethys Himalayan Subzone, southern Tibet, China. The CORB, which is called as the Chuangde Formation, in Gyangze area is mainly composed of micofossil-bearing red limestone and shale intercalated with siliceous rock (chert). This study focuses on the planktic foraminiferal biostratigraphy of the CORB in Gyangze area, Southern Tibet, China.

Material and Methods

A detailed geologic survey was carried out on the Upper Cretaceous, especially the CORBs, in the Gyangze area, southern Tibet (Figure 1). Samples mainly of limestone and shale were collected from the Chuangde Formation (CORBs) mainly to uncover planktic foraminiferal fossils.

Samples were processed in various ways according to different lithology and hardness as follows: For relatively soft samples such as shale, about 100 g from each sample were soaked with a 10% Na2SO4 solution, washed over a 50 μm mesh sieve and dried and sieved into fractions greater than 250μm, 80 μm and 50 μm, respectively. About 50 g of washed residue was then examined. For hard samples, such as limestone, numerous thin-sections (especially axial sections of foraminifera) were prepared for taxonomic analysis and were cut in different orientations after visual observations. All rock samples, fossils and thin sections are housed at the Fossil Identification Center, the China University of Geosciences (Beijing).

Planktic Foraminiferal Biostratigraphy

With few exceptions, the well-preserved foraminifera from the the CORBs of the Gyangze area fossils can be identified to genus or species level. Established Cretaceous planktic foraminiferal biostratigraphy was applied to this study using age assignments for planktic zones of Caron [10] and Nederbragt [11].

The foraminiferal assemblages are dominated by such genera as (Figure 1): Archaeoglobigerina, Contusotruncana, Dicarinella, Hedbergella, Heterohelix, Globotruncana, Globotruncanita, Globigerineloides, Marginotruncana, Radotruncana, and Rugoglobigerina. The important elements of the planktic foraminiferal assemblage include Archaeoglobigerina bowi, Globigerilloides ultramicra, G.prairiehillensis, Globotruncana linneiana, G. lapparenti, G. arca, G.ventricosa, G. falsostuarti, Globotruncanella havanensis, Globotruncanita elevata, G. stuartiformis, G. stuarti, Hedbergella holmdelensis, Heterohelix globulosa, H. striata, Radotruncana calcarata, and R. subspinosa etc. Four planktonic foraminiferal biozones were recognized (in ascending order) G. elevata, G. ventricosa, R. calcarata and G. havanensis zones, which provided the Chuangde Formation (CORB) with an age of Late Cretaceous Campanian.

Figure 1: The representative elements of the planktic foraminiferal assemblage from the Chuangde Formation (CORB) in Gyangze area, Tibet. 1. Archaeoglobigerina blowi (Pessagno, 1967)(CW100-40); 2. Archaeoglobigerina cretacea (d’Orbigny, 1840)(CW74-31); 3,4,9. Globotruncanita stuarti (De Lapparent, 1951)(3.CW100-124; 4.CW102-12b; 9. CW74-66); 5. Contusotruncana fornicata (Plummer,1931)(5. CW74-222; 6. CW90-74;7.CW74-238 ; 8.CW81-45); 9. Globotruncanita stuatiformis (Dalbiez, 1955)(CW74- 25); 10,11. Globotruncana linneiana (d’Orbigny, 1839) (10. CW85-118; 11. CW85-153); 12, 13. Globotruncana bulloides (Vogler, 1941)(12.CW85-136; 13. CW102-14); 14-16. Globotruncana arca (Cushman, 1926)(14.CW83-50;15.CW102-29; 16.CW37- 36); 17,18. Globotruncana ventricosa (White,1928) (17.CW31-21; 18. CW31-26); 19. Globotruncanita elevata (Brotzen, 1934) (CW30-71); 20. Globotruncana lapparenti (Brotzen, 1936) (CW98-40); 21. Rodotruncana calcarata (Cushman, 1927) (CW102- 1); 22-24. Globotruncanita stuatiformis (Dalbiez, 1955) (22. CW81-63; 23. CW74-58; 24.CW74-25).
Click to enlarge
Figure 1: The representative elements of the planktic foraminiferal assemblage from the Chuangde Formation (CORB) in Gyangze area, Tibet. 1. Archaeoglobigerina blowi (Pessagno, 1967)(CW100-40); 2. Archaeoglobigerina cretacea (d’Orbigny, 1840)(CW74-31); 3,4,9. Globotruncanita stuarti (De Lapparent, 1951)(3.CW100-124; 4.CW102-12b; 9. CW74-66); 5. Contusotruncana fornicata (Plummer,1931)(5. CW74-222; 6. CW90-74;7.CW74-238 ; 8.CW81-45); 9. Globotruncanita stuatiformis (Dalbiez, 1955)(CW74- 25); 10,11. Globotruncana linneiana (d’Orbigny, 1839) (10. CW85-118; 11. CW85-153); 12, 13. Globotruncana bulloides (Vogler, 1941)(12.CW85-136; 13. CW102-14); 14-16. Globotruncana arca (Cushman, 1926)(14.CW83-50;15.CW102-29; 16.CW37- 36); 17,18. Globotruncana ventricosa (White,1928) (17.CW31-21; 18. CW31-26); 19. Globotruncanita elevata (Brotzen, 1934) (CW30-71); 20. Globotruncana lapparenti (Brotzen, 1936) (CW98-40); 21. Rodotruncana calcarata (Cushman, 1927) (CW102- 1); 22-24. Globotruncanita stuatiformis (Dalbiez, 1955) (22. CW81-63; 23. CW74-58; 24.CW74-25).

Figure 1: The representative elements of the planktic foraminiferal assemblage from the Chuangde Formation (CORB) in Gyangze area, Tibet. 1. Archaeoglobigerina blowi (Pessagno, 1967)(CW100-40); 2. Archaeoglobigerina cretacea (d’Orbigny, 1840)(CW74-31); 3,4,9. Globotruncanita stuarti (De Lapparent, 1951)(3.CW100-124; 4.CW102-12b; 9. CW74-66); 5. Contusotruncana fornicata (Plummer,1931)(5. CW74-222; 6. CW90-74;7.CW74-238 ; 8.CW81-45); 9. Globotruncanita stuatiformis (Dalbiez, 1955)(CW74- 25); 10,11. Globotruncana linneiana (d’Orbigny, 1839) (10. CW85-118; 11. CW85-153); 12, 13. Globotruncana bulloides (Vogler, 1941)(12.CW85-136; 13. CW102-14); 14-16. Globotruncana arca (Cushman, 1926)(14.CW83-50;15.CW102-29; 16.CW37- 36); 17,18. Globotruncana ventricosa (White,1928) (17.CW31-21; 18. CW31-26); 19. Globotruncanita elevata (Brotzen, 1934) (CW30-71); 20. Globotruncana lapparenti (Brotzen, 1936) (CW98-40); 21. Rodotruncana calcarata (Cushman, 1927) (CW102- 1); 22-24. Globotruncanita stuatiformis (Dalbiez, 1955) (22. CW81-63; 23. CW74-58; 24.CW74-25).

Globotruncanita elevata zone

The Globigerinelloides elevata Zone is a partial range zone (PRZ) after Postuma [12], and it spans the interval from the LO of D. asymetrica to the FO of G. ventricosa. In Gyangze area, The key species of this zone ranges include: Archeoglobigerina blowi, Globigerinelloides prairiehillensis, G. ultramicra, Globotruncana arca, G. bulloides, G. carinata, G. lapparenti, G. linneiana, Globotruncanita elevata, G. stuartiformis, Heterohelix carinata, H. cordites, H. globulosa, H. planata, H. reussi, H. striata, Laeviheterohelix pulchara, Marginotruncana coronata, M. marginata, Planoglobulina ornatissima. The age of this zone is early Campanian.

Globotruncana ventricosa zone

The Globotruncana ventricosa Zone is a partial range zone (PRZ) defined by Dalbiez [13], and is marked by the FOs of G. ventricosa and R. calcarata at its base and top, respectively. In Gyangze, this zone is defined by the FO of G. ventricosa at its base and by the FO of R. calcarata at its top. Key elements include: Globigerinelloides prairiehillensis, Globotruncana arca, G. bulloides, G. carinata, G. falsostuarti, G. lapparenti, G. linneiana, G. rosseta, G. ventricosa, Globotruncanita stuarti, G. stuartiformis, Hedbergella holmdelensis, Heterohelix americana, H. carinata, H. cordites, H. grabrans, H. globulosa, H. reussi, H. striata, Pseudotextularia nuttalli, Rugoglobigerina rugosa, and Schackoina multispinata. This zone is dated as early Campanian to middle Campanian in age.

Radotruncana calcarata zone

The Radotruncana calcarata Zone is a total range zone (TRZ) described by Herm [14], which spans the total range of R. calcarata. In Gyangze, the base and top of this zone are marked respectively by the FO and LO of R. calcarata. Important elements include planktic species: Archaeoglobigerina blowi, A, cretacea, Contusotruncana sp., Globigerineloides prairillensis, Globotruncana aegyptiaca, G. arca, G. carinata, G. bulloides, G. globigerilloides, G. linneiana, G. mariei, G. rosseta, G. ventricosa, Globotruncanella havanensis, Globotruncanita stuarti, G. stuartiformis, Heterohelix carinata, H. cordatus, H. globulosa, H. reussi, H. striata, Laeviheterohelix dentata, L. pulchara, L. turgita, Pseudotextularia nuttalli, Radotruncana calcarata, R. subspinosa, Rugoglobigerina rugosa, and Schackoina multispinata. The age of this zone is inferred as middle Campanian.

Globotruncanella havanensis zone

The Globotruncanella havanensis Zone is a partial range zone (PRZ) defined by Caron [15], with Globotruncanella havanensis, from LO of R. calcarata to the FO of Globotruncana aegyptiaca. In Gyangze, the base of this zone is defined by the FO of R. calcarata. Representative elements of this zone include Globotruncanella havanensis, Globotruncana bulloides, G. linneiana, G. ventricosa, Globigerinelloides prairiehillensis, Archaeoglobigerina blowi, A. cretacea, Heterohelix sp., H. striata and Contusatruncana fornicata. The age of this zone is inferred as late Campanian.

Discussion

Age assignment

This paper mainly adopts the Cretaceous planktic foraminiferal zonal schemes of Caron (1985). Globotruncana ventricosa, which defines the G. ventricosa Zone, is Campanian to Maastrichtian in age. G. stuarti ranges from the late Campanian to the end of Maastrichtian, i.e., from the middle of G. havanensis Zone to the top of A. mayaroensis Zone. G. stuartiformis is restricted to the latest Santonian to Late Maastrichtian, i.e., from the top of D. asymmetric Zone to the lower A. mayaroensis Zone. Heterohelix globulosa ranges from the earliest Campanian to Middle Maastrichtian. Contusatruncana fornicata ranges from Middle Santonian to Middle Maastrichitian. Radotruncana calcarata defines the R. calcarata Zone, which is limited to middle Campanian. Globotruncanella havanensis, which defines the G. havanesis Zone, is late Campanian to the end of Maastrichtian in age.

Palaeogeographic distribution of CORBs

Cretaceous strata in Tethyan Himalaya of southern Tibet have been considered as deposits from the northern Indian passive margin. In general, Upper Cretaceous strata from the southern Tethyan Himalaya record shallow to deep shelf environments, while time-equivalent units from the northern Tethyan Himalaya document continental slope to basinal environments [3, 4, 5, 6, 8, 16, 17, 18, 19, 20, 21].

The “Cretaceous Oceanic Red Beds (CORBs)” associated with “Oceanic Oxic Events” have become a hot topic for geologists from around the world. In southern Tibet, Upper Cretaceous oceanic red beds (CORBs) are widely distributed in the northern Tethyan Himalayas [3, 4, 5, 6, 8, 9, 20, 21] (Figure 2). These CORBs are composed of pink limestone, marl, shale, siltstone, and radiolariants (siliceous rocks, usually assigned to the Chuangde Formation. The origin of these CORBs remains uncertain, but most authors believe that they are related to change in ocean circulation patterns and low deposition rates [8, 20, 21].

Figure 2: Distribution and stratigraphic correlation of the CORBs in the Tethyan Himalayan area (modified from Li, et al, [3]; Li, et al. [22]; Gansser [23]).
Click to enlarge
Figure 2: Distribution and stratigraphic correlation of the CORBs in the Tethyan Himalayan area (modified from Li, et al, [3]; Li, et al. [22]; Gansser [23]).

Paleogeographic reconstruction [3, 4] shows that the CORBs represented by the Chuangde Formation and its time- equivalent units are confined to the deep water environments and are completely absent in the shelf environments including shelf margin. Given the similar stratigraphic thickness of shelf and slope/basin sections, it is unlikely that the Tethy-Himalayan CORBs were formed by terrigenous iron transport to a sediment-deficient ocean.

Recently, our field geological survey [22] found a shallow-marine purple limestone layer with the thickbess of 5 m, equivalent to the CORB, in the Cretaceous Zongshan Formation of the Gyabukeqing section of Yadong, southern Tethyan Himalayas, which is the first report of the shallow- marine CORB in a shelf setting.

Conclusion

The study on the planktic foraminiferal biostratigraphy of the CORBs developed in Gyangze area, northern Tethyan Himalayas, southern Tibet were carried out. Four planktonic foraminiferal biozones were recognized (in ascending order) G. elevata, G. ventricosa, R. calcarata and G. havanensis zones, which provided the Chuangde Formation (CORB) with an age of Late Cretaceous Campanian.

Acknowledgments

This work is granted by the National Natural Science Foundation of China (Grant No. 41272030), the IGCP679, and the National Basic Research Program of China (Grant No. 2012CB822001).

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@article{yuewei2021,
  title   = {Planktic Foraminiferal Biostratigraphy of the Cretaceous Oceanic Red Beds in Gyangze, Tibet},
  author  = {Yuewei L, Chengshan W, Guobiao L, Jinbiao Z, Jingjing W and Kezhantu B},
  journal = {International Journal of Paleobiology & Paleontology},
  year    = {2021},
  volume  = {4},
  number  = {1},
  doi     = {10.23880/ijpbp-16000127}
}
Yuewei L, Chengshan W, Guobiao L, Jinbiao Z, Jingjing W and Kezhantu B (2021). Planktic Foraminiferal Biostratigraphy of the Cretaceous Oceanic Red Beds in Gyangze, Tibet. International Journal of Paleobiology & Paleontology, 4(1). https://doi.org/10.23880/ijpbp-16000127
TY  - JOUR
TI  - Planktic Foraminiferal Biostratigraphy of the Cretaceous Oceanic Red Beds in Gyangze, Tibet
AU  - Yuewei L, Chengshan W, Guobiao L, Jinbiao Z, Jingjing W and Kezhantu B
JO  - International Journal of Paleobiology & Paleontology
PY  - 2021
VL  - 4
IS  - 1
DO  - 10.23880/ijpbp-16000127
ER  -