03/06/19

The use of 28,30-Bisnorhopane as a stratigraphic marker

by Laura Garner

The demethylated hopane 17α,21β(H)-28,30-bisnorhopane (Figure 1) is a compound regularly used as a stratigraphic marker, particularly for Upper Jurassic source rocks and associated expelled oils within the North Sea and Norwegian Sea; however, there is still very little known of its origin.

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Figure 1. Molecular structure of 28,30-Bisnorhopane and identification on m/z 191 GC-MS trace.

Seifert et al. (1978) proposed several fern constituent precursors such as adipedatol, adiantone and 21-hydroxyadiantone (Figure 2). The possibility of an enrichment in bisnorhopane due to a molecular sieve effect in nature (due to pore size of the inorganic matrix) was also suggested by these authors but is no longer considered. Grantham et al. (1980) identified small concentrations of bisnorhopane within pre-Devonian source rock extracts and related crude oils. Ferns are not thought to have existed prior to the Devonian, and therefore the formation of the hopane from such precursors is unlikely unless produced by an unknown organism active during the depositional environment of the source rocks.

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Figure 2. Molecular structure of adipedatol and adiantone, potential precursors of 28,30-bisnorhopane.

A more widely accepted theory of a chemoautotrophic bacteria precursor has been proposed by numerous authors. Katz & Elrod (1983) identified an inverse correlation between the increasing abundance of bisnorhopane and decreasing pristane/phytane ratio, suggesting that bisnorhopane concentration is related to a strongly anoxic depositional environment. Schoell et al. (1992) used compound specific isotope analysis (CSIA) to determine the likely bacterial origin of 28,30-bisnorhopane. The isotopic signatures of the bisnorhopane stereoisomers within the immature Monterey-sourced oils are between 8-9‰ lighter than the whole oil, and around 6-8‰ lighter than other hopane compounds (Figure 3). This suggests that the precursor of bisnorhopane occupied a specific and different ecological niche compared to other hopane-synthesising organisms. The depletion in δ13C within bisnorhopane requires biosynthesis by an organism that utilises δ13C-depleted substrates, namely chemoautotrophic bacteria such as nitrifying and/or sulphur-oxidising species.

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Figure 3. (Adapted from Schoell et al., 1992) Stable carbon isotopic composition of 28,30-bisnorhopane and other hopane biomarkers in Monterey crude oil.

An unusual aspect of 28,30-bisnorhopane is that it is not found as part of the kerogen structure (as regular hopanes are) but is present only as a free (solvent-soluble) compound within the rock, as highlighted by Noble et al. (1985). Conducted pyrolysis experiments only yielded the common hopane and moretane series, indicating that the bisnorhopane (or its precursors) have not been part of the organic material incorporated into the kerogen matrix. At increasing levels of thermal maturity, the generation and release of hydrocarbons (containing regular hopanes) from the kerogen, results in the dilution of bisnorhopane, which explains why lower relative abundances of bisnorhopane are evident within crude oils compared to source rocks. Bisnorhopane/hopane ratios are therefore only a useful correlation parameter when samples have similar thermal maturities.

Both facies composition and thermal maturity therefore have important controls over the presence and abundance of bisnorhopane within oils and source rocks. Grantham et al. (1980) and Mackenzie et al. (1983) identified decreasing bisnorhopane content with decreasing organic sulphur content (the latter being shown to decrease as crudes are generated from increasingly more mature source rocks), indicating that potentially thermal maturity is the biggest factor in bisnorhopane abundance in fluids. Conversely, Hughes et al. (1985) indicated the opposite trend to both Grantham and Mackenzie, in that relative bisnorhopane contents increased with decreasing sulphur contents (Figure 4), suggesting that concentrations are likely more facies controlled than due to thermal maturity.

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Figure 4. (Adapted from Hughes et al., 1985) Increasing bisnorhopane/hopane ratio to decreasing sulphur (wt.%) within greater Ekofisk crude oils.

It is important to note that although 28,30-bisnorhopane is typically associated with anoxic Upper Jurassic source rocks such as the Kimmeridge Clay Formation (KCF), this compound is not universally present in this stratigraphic interval. Dahl (2004) used 28,30-bisnorhopane as a stratigraphic marker in the North Viking Graben of the Norwegian North Sea, where higher relative amounts of bisnorhopane characterise the older “syn-rift” section of the Upper Jurassic Draupne Formation, with little to no bisnorhopane present within the younger “post-rift” Draupne section. Dahl & Speers (1985) and Schou et al. (1985) presented a marked absence of bisnorhopane in the KCF, with the former author highlighting the presence of the compound in the older Heather Formation. This supports that although bisnorhopane can be used as a stratigraphic marker, its absence does not exclude sourcing from the Upper Jurassic in the North and Norwegian Sea.

 

References

Dahl, B. (2004) The use of bisnorhopane as a stratigraphic marker in the Oseberg Back Basin, North Viking Graben, Norwegian North Sea. Organic Geochemistry35(11-12): 1551-1571.

Dahl, B. & Speers G. C. (1985) Organic geochemistry of the Oseberg Field (I). Petroleum Geochemistry in Exploration of the Norwegian Shelf. B. M. Thomas and et al. London, Graham and Trotman Ltd.: 185-196.

Grantham, P. J., et al. (1980) Variation and significance of the C27 and C28 triterpane content of a North Sea core and various North Sea crude oils. Physics and Chemistry of The Earth12: 29-38.

Hughes, W. B., et al. (1985) Geochemistry of Greater Ekofisk crude oils. Petroleum Geochemistry in Exploration of the Norwegian Shelf. B. M. Thomas and et al. London, Graham and Trotman Ltd.: 75-92.

Katz, B. J. and L. W. Elrod (1983) Organic geochemistry of DSDP Site 467, Offshore California, Middle Miocene to Lower Pliocene strata. Geochimica et Cosmochimica Acta 47: 389-396.

Mackenzie, A. S. and J. R. Maxwell (1983) Biological marker and isotope studies of North Sea crude oils and sediments. World Petroleum Congress, 11th World Petroleum Congress, 28 August-2 September, London, UK.

Moldowan, J.M., Seifert, W.K., Arnold, E., Clardy, J. (1984) Structure proof and significance of stereoisomeric 28,30-bisnorhopanes in petroleum and petroleum source rocks. Geochimica et Cosmochimica Acta 48: 1651-1661.

Noble, R., et al. (1985) The occurrence of bisnorhopane, trisnorhopane and 25-norhopanes as free hydrocarbons in some Australian Shales. Organic Geochemistry 8(2): 171-176.

Schoell, M., et al. (1992) Carbon isotopic compositions of 28,30-bisnorhopanes and other biological markers in a Monterey crude oil. Geochimica et Cosmochimica Acta56(3): 1391-1399.

Schou, L., et al. (1985) Oil-oil and oil-source rock correlation, northern North Sea. Petroleum Geochemistry in Exploration of the Norwegian Shelf. Proceedings of a Norwegian Petroleum Society (NPF) Conference held in Stavanger 22-24 October 1984. B. M. Thomas and et al. London, Graham and Trotman Ltd.: 101-117.

Seifert, W. K., et al. (1978) First proof of structure of a C28-pentacyclic triterpane in petroleum. Nature271: 436-437.

 

 

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