1. Introduction
The Jurassic–Cretaceous transition is a known period of significant environmental perturbations, the frequency and magnitude of which remain poorly understood. (Tennant et al. Reference Tennant, Mannion, Upchurch, Sutton and Price2017 and references within). During the Tithonian and Valanginian two significant sea level falls of ~40 m occurred (Haq Reference Haq2014), reducing marine connectivity resulting in the establishment of unique bioprovinces reflecting spatial and temporal differences in marine flora and fauna. The intricate relationship between marine phytoplankton and climate allows for the utilisation of dinoflagellate cysts as a palaeoenvironmental proxy (e.g., Dypvik & Harris, Reference Dypvik and Harris2001; Retallack, Reference Retallack2008; Davies et al. Reference Davies, Lamb, Roberts, Croudace and Rothwell2015), which is used to decipher the interplay of long term and short term climate fluctuations, distinguishing them from evolutionary signals. Dinoflagellate cyst morphological trends are of particular importance across the Jurassic–Cretaceous transition, as a major shift to chorate cysts across the Arctic is observed (e.g., Lebedeva & Nikitenko, Reference Lebedeva and Nikitenko1999; Nøhr-Hansen et al. Reference Nøhr-Hansen, Piasecki and Alsen2019; Sliwińska et al. Reference Sliwinska, Jelby, Grundvåg, Nøhr-Hansen, Alsen and Olaussen2020; Ingrams et al. Reference Ingrams, Jolley and Schneider2021).
The Rollrock Section, Arctic Canada, is one of the highest palaeolatitude continuous sections spanning the Jurassic–Cretaceous transition, and the northernmost section in the Sverdrup Basin (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020; Ingrams et al. Reference Ingrams, Jolley and Schneider2021). Previous palynological studies of assemblages recovered from the basin focused entirely on biostratigraphy (Ingrams et al. Reference Ingrams, Jolley and Schneider2021) and/or had less complete sections, lower sample numbers or more widely spaced samples (Davies Reference Davies1983; Galloway et al. Reference Galloway, Sweet, Swindles, Dewing, Hadlari, Embry and Sanei2013, Reference Galloway, Tullius, Evenchick, Swindles, Hadlari and Embry2015; Nguyen et al. Reference Nguyen, Galloway, Poulton and Dutchak2020). More recent palynological analysis of the basin has been undertaken on incomplete or slightly more southern sections and focused on terrestrial rather than marine floras (Galloway et al. Reference Galloway, Sweet, Swindles, Dewing, Hadlari, Embry and Sanei2013, Reference Galloway, Tullius, Evenchick, Swindles, Hadlari and Embry2015, Reference Galloway, Vickers, Price, Poulton, Grasby, Hadlari, Beauchamp and Sulphur2020). This study combines the results of modern palynological processing techniques with a quantitative multivariate statistical approach, to provide an improved understanding of fluctuating marine floral assemblages and palaeoclimatic trends across the Jurassic–Cretaceous boundary in the Sverdrup Basin. The terrestrial component of the recovered assemblages has been analysed separately (work in progress). Based on the recovered pattern, a framework of third order and fourth order depositional sequences is established for the transition interval.
Continuous exposures across the Jurassic–Cretaceous transition at high palaeo-latitudes is rare (e.g., Jelby et al. Reference Jelby, Śliwińska, Koevoets, Alsen, Vickers, Olaussen and Stemmerik2020 and references within). Therefore, the mudstones of the Rollrock Section provide an ideal archive for palynomorph assemblages from across the Jurassic–Cretaceous transition. Palynomorphs occur continuously over the succession, enabling multivariate quantitative statistical analyses. These analyses in turn provide statistical evidence for environmental controls over marine phytoplankton assemblages.
2. Geological setting
The Sverdrup Basin is located within the Canadian Arctic Islands, encompassing an area of ~300,000 km2 (Balkwill Reference Balkwill1978; Embry & Beauchamp Reference Embry, Beauchamp and Miall2019; Fig. 1). Basin development began in the Early Carboniferous on a basement of Neoproterozoic–Devonian sedimentary strata, terminating in the latest Cretaceous with the Eurekan Orogeny (Hadlari et al. Reference Hadlari, Midwinter, Galloway, Dewing and Durbano2016; Embry & Beauchamp Reference Embry, Beauchamp and Miall2019).
Since development began, 13–15 km of sedimentary strata were deposited which have been assigned to eight significant, unconformity-bound phases of deposition (Embry & Beauchamp Reference Embry, Beauchamp and Miall2019). The Oxfordian–Valanginian strata studied herein were deposited during the fifth phase (Rhaetian–mid-Valanginian), a period characterised by relatively shallow marine deposition. The sedimentary rocks of the middle and latter portions of this phase (Pliensbachian–mid-Valanginian) were deposited in a syn-rift setting (Hadlari et al. Reference Hadlari, Midwinter, Galloway, Dewing and Durbano2016), climaxing around the Jurassic–Cretaceous transition, which is the main focus of this study. During this phase, more distal locations, such as the Rollrock Section, were dominated by mud deposition, with sands representing only the most severe regressive phases.
2.1. Lithostratigraphy
The studied section, initially described by Wilson (Reference Wilson1976), crops out on the northern slope of the Rollrock River Valley on Northern Ellesmere Island, extending over 5 km laterally (Fig. 1). The logged and sampled section is a 560 m thick continuous exposure of Late Jurassic–Early Cretaceous sedimentary rock. The base of the logged section is located near 81.61172°N, −75.58489°W with the top near 81.617447°N, −75.596306°W; WGS84 datum (detailed log in Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). The Rollrock Section begins with the Ringnes Formation, a thick succession of dark, thinly bedded or laminated mudstones and siltstones, with rare intercalations of fine-grained sandstones, becoming more abundant in the uppermost 20 m of the unit. This interval was previously assigned to the Awingak Formation by Embry (in Mayr and Trettin, Reference Mayr and Trettin1996), but is not sand dominated and thus does not conform to the lithological definition of this unit. Nevertheless, the sandstone horizons are likely a distal representation of the Sildre Member of the Awingak Formation (see Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020 for details). Palynological and macrofossil investigations give an Oxfordian to (early) Tithonian age for the Ringnes Formation (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020; Ingrams et al. Reference Ingrams, Jolley and Schneider2021).
Location map of the Sverdrup Basin (a). Geology of the Sverdrup Basin (after Harrison et al. Reference Harrison, St-Onge, Petrov, Strelnikov, Lopatin, Wilson, Tella, Paul, Lynds, Shokalsky, Hults, Bergman, Jepsen, Numerical and Solli2011) (b). Location of the Rollrock Section on Ellesmere Island (star), (modified from Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020).
At 251 m, there is a sharp contact between the fine-grained sandstones and overlying mudstones. This change in lithology marks the boundary between the Ringnes and Deer Bay formations (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). The Deer Bay Formation consists of dark, thinly bedded or laminated mudstones. A sandstone bed containing large concretions at 273 m and a thin indurated siltstone interval are the only interruptions to mudstone deposition. Palynological and macrofossil evidence gives a Tithonian–Valanginian age for the Deer Bay Formation (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020; Ingrams et al. Reference Ingrams, Jolley and Schneider2021). Eight horizons of glendonites, which have been described as the most distinguishing aspect of the upper Deer Bay Formation by Kemper (Reference Kemper1975), have been recorded from the upper part of the Rollrock Section (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), and palynological evidence identifies these as Valanginian in age (Ingrams et al. Reference Ingrams, Jolley and Schneider2021).
Beginning at 520 m there are frequent intercalations of siltstone and, very-fine to fine grained sandstone horizons. A clean, trough cross-bedded sandstone occurring at 524.5 m indicates a lithological switch to a sand dominated succession. This change in lithofacies has been interpreted as the boundary between the Deer Bay Formation and the Isachsen Formation (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). The latter is generally defined as a succession of light coloured quartzose sandstone and conglomerates, with interbeds of dark siltstone, shale, and coal (e.g., Embry, Reference Embry1985; Galloway et al. Reference Galloway, Tullius, Evenchick, Swindles, Hadlari and Embry2015). Only one sample was taken from a shale interval in the Isachsen Formation at 537 m and as such, this unit is not the main focus of this study.
2.2. Chronostratigraphy
The study area lacks an accurate geochronostratigraphical framework. Consequently, the ages of the formations have been constrained using a combination of macropalaeontology and palynology (Galloway et al. Reference Galloway, Tullius, Evenchick, Swindles, Hadlari and Embry2015, Reference Galloway, Vickers, Price, Poulton, Grasby, Hadlari, Beauchamp and Sulphur2020; Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020; Ingrams et al. Reference Ingrams, Jolley and Schneider2021). Ammonites are the most stratigraphically useful macrofossils, but fossiliferous horizons yield low abundances and are widely spaced across the Jurassic and Cretaceous. Ammonites combined with Buchia bivalves have been used to create a chronological framework for the basin (Jeletzky Reference Jeletzky1984; Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), which was utilised when examining the distribution of palynomorphs in the Rollrock Section, culminating in a new palynological biostratigraphic scheme for the region (Ingrams et al. Reference Ingrams, Jolley and Schneider2021). The result of these studies is that the Rollrock section is now the stratigraphically best constrained section spanning the Jurassic–Cretaceous transition in the Sverdrup Basin.
3. Dinoflagellate cyst functional morphology
Fossil dinoflagellate cysts have been subdivided into three broad categories defined by process length as a percentage of the shortest diameter of the central body (Sarjeant Reference Sarjeant1982). By definition, process length in proximate cysts is less than 10%, in proximochorate cysts between 10% and 30%, and in chorate cysts greater than 30%. While this differentiation is arbitrary and cyst placement into these three categories can vary between authors (due to intraspecific variability in process length), it is still useful in palaeoenvironmental interpretations.
Dinoflagellates have evolved three key strategies enabling them to survive: they are good competitors; stress-tolerant; and disturbance-tolerant. This allows them to exist in a wide-ranging variety of aqueous and sea ice environments (Reynolds Reference Reynolds and Sommer1989; Smayda & Reynolds Reference Smayda and Reynolds2001, Reference Smayda and Reynolds2003). Investment in rapid development and reproduction enhances innate competitive ability. Resting cyst stages allow dinoflagellates greater control over when blooming occurs, with cysts remaining docile for up to 10 years if environmental conditions are not adequate for excystment (Smayda Reference Smayda2002). This is one reason dinoflagellates are not as affected by global extinction events such as the Cretaceous–Palaeogene boundary (e.g., Galeotti et al. Reference Galeotti, Brinkhuis and Huber2004). Stress tolerance enables species to survive and function in severely nutrient depleted environments, including Arctic environments with highly seasonal climates, where polar winter brings darkness and colder temperatures, resulting in a diminished nutrient supply. Disturbance tolerance allows species to withstand frequent or continuous turbulence in shallow marine environments. These adaptations are not uniform across all dinoflagellate species, as some are able to tolerate higher levels of stress than others (Smayda & Reynolds Reference Smayda and Reynolds2003).
4. Methods
4.1. Study area
All sampled material was collected from the Rollrock Section (Figs 1, 2). Samples were selected from shale beds in the basal 355 m of the section using a combined targeted and systematic approach. However, gaps of no more than 9 m were left unsampled (n = 90, AVE = 3.98 m.). The top 168 m yielded higher quality preservation and as such were sampled at 1.5 m density (n = 109). Three samples located at 474 m, 502.5 m and 504 m were lost during transport. A single sample was prepared from the overlying Isachsen Formation at 537 m.
Selected palynomorphs from the Rollrock Section, Sverdrup Basin. Scale bar represents 20 μm. (a) Tubotuberella rhombiformis 384 m (V31). (b) Pareodinia borealis 132 m (U19-4). (c) Tanyosphaeridium isocalamum 408 m (T26). (d) Gonyaulacysta adecta 19.5 m (W29-3). (e) Muderongia simplex 505.5 m (V32-3). (f) Nelchinopsis kostromiensis 469.5 m (T37-4). (g) Tanyosphaeridium magneticum 406.5 m (U24-1). (h) Rhynchodiniopsis cladophora 19.5 m (V25-1). (i) Chytroeisphaeridia chytroeides 411 m (T30-3). (j) Sentusidinium separatum 361.5 m (V21-1). (k) Trichodinium erinaceoides 372 m (W33). (l) Oligosphaeridium complex 487.5 m (V26-2). (m) Paragonyaulacysta capillosa 195 m (D24-2). (n) Gochteodinia villosa villosa 487 m (U21-2). (o) Muderongia tetracantha 522 m (H23). (p) Gochteodinia villosa 402 m (T22).
4.2. Laboratory processing
Selected samples were prepared using hydrofluoric (HF) and hydrochloric acid (HCl) maceration. 114 samples were prepared by MB Stratigraphy Ltd. and 86 samples were prepared in the University of Aberdeen. Preparations were done concurrently using the same technique outlined below.
Samples were lightly broken apart and then demineralised using HF. HCl was used to remove any carbonates and HF precipitate. The remaining organic component was concentrated by a combination of nitric oxidation (by Schultze solution) and swirling techniques. Where necessary samples were processed in a centrifuge for heavy liquid separation. This was done by the sodium-polytungstate (3Na2WO4⋅9WO3) method with the inorganic compound made up to a specific gravity of 2.2.
The remaining organic component was strewn onto a glass slide and analysed under a microscope. A count of 250 marine palynomorphs was aimed for. In samples with poor recovery, the entire slide was analysed. In samples with recovery greater than 250, the remaining slide was analysed for additional, rare taxa, which were recorded outside of the count.
Portable X-ray fluorescence (PXRF) analysis was undertaken using an Olympus Delta Premium handheld XRF analyser, housed in the University of Aberdeen. Prior to analysis approximately 10–15 g of all samples were ground into a fine powder using a pestle and mortar. The grinding process homogenised the samples creating a flat surface and sufficient depth to enable measurements to be accurately taken. After powdering samples were carefully transferred into a glass vial. The vial lids were removed and replaced by a thin layer of non-polyvinyl chloride cling film. These vials were then inverted and transferred into the Delta PXRF workstation containing the PXRF analyser, taking care to line the analyser aperture up with the centre of the powder to prevent the glass of the vial being analysed.
4.3. Multivariate techniques
Multivariate statistical analyses are based on quantitate data of marine dinoflagellate cysts preserved in the Rollrock Section across the Ringnes, Deer Bay, and Isachsen Formations (Appendix 1 available at https://doi.org/10.1017/tre2200008). The computer software program PAST (Hammer et al. Reference Hammer, Harper and Ryan2001; Hammer & Harper Reference Hammer and Harper2006) was used for Q-mode hierarchical cluster analysis, which grouped similar samples together, providing the basis for palaeoenvironmental interpretations. The algorithm ‘Ward's method’ that joins clusters such that increase in within-group variance is minimised, was used. These analyses create dendrograms, clustering samples based on palynomorph content, joining similar pairs to a common node, with branch lengths indicating relative similarities (Paliy & Shankar Reference Paliy and Shankar2016). Ward's method uses Euclidean distance, which assumes simplified linear relationships producing quick visuals of similarities between variables. Therefore, these clusters can be used to make broad interpretations about the samples and also provide a basis for further analytical statistical techniques.
The computer software program PAST was also utilised for detrended correspondence analysis (DCA). DCA is a multivariate statistical technique used to interpret species and sample ordination (Hill & Gauch Reference Hill and Gauch1980). DCA was created by Hill (Reference Hill1979) in order to compensate for the ‘arch’ and ‘edge’ effects inherent in other multivariate techniques such as principal component analysis (PCA). The arch (horseshoe) effect is the two-dimensional mathematical presentation of ecological data as a curve rather than a straight line, due to axis two in PCA being both uncorrelated with and dependent on axis one (Hill & Gauch Reference Hill and Gauch1980). To make accurate interpretations about these axes, they need to be uncorrelated and independent of one another. The edge effect is produced when compositional distances are not preserved. Two pairs of samples with the same compositional distances will exhibit two different distances in the ordination, depending on where they are located on the first axis, resulting in compositional differences appearing greater in the middle of the gradient than at the ends (Hill & Gauch Reference Hill and Gauch1980). DCA overcomes the arch effect by dividing the first axis into segments, and then rescaling its axes, so the values on the second axis are equalised to a zero mean value. Rescaling ensures that equal compositional differences are represented by equal differences along the gradient, eliminating the edge effect (Hill & Gauch Reference Hill and Gauch1980).
The DCA was favoured herein over other multivariate techniques because floras, and their environment, usually have a non-monotonic and unimodal relationship rather than a linear one. DCA is also more suitable when dealing with zero data than PCA (Paliy & Shankar Reference Paliy and Shankar2016). This becomes important when analysing long stratigraphic sections with frequent extinction and inception events controlled by time and environmental factors. DCA arranges data along two principal axes that represent variables such as environmental factors. The eigenvalues associated with each axis depict the extent to which each axis influences the data (Ramette Reference Ramette2007). Therefore, DCA can be utilised to observe and interpret species distribution and sample variation without the distortion seen in other multivariate techniques.
Correspondence analysis (CA) is an ordination method that can be used to display ecological information, which is inferred from axes of eigenvalues representing directions of variation in a given assemblage data set. The eigenvalues derived are coefficients reflecting the degree of species dispersion along the axes (Ter Braak Reference Ter Braak1986; Kovach Reference Kovach1993).
Canonical correspondence analysis (CCA) is an extension of CA, in which an additional matrix, in this case of environmental data, is included in the analysis. Ordination axes (vectors) are added for known (environmental) variables (Ter Braak Reference Ter Braak1986; Kovach Reference Kovach1993). For example, this study uses elemental ratios derived from PXRF analysis.
Prior to undertaking statistical analyses, the data were processed to reduce statistical noise, resulting in more viable results. Firstly, samples with a count size of 25 or less (≤10% of highest count) were removed. This resulted in the removal of 13 samples. Secondly, taxa counts were converted into percentages to account for varying count sizes. Implementation of these techniques removed bias in the data towards taxa present in sparse and abundant samples. Consequently, these taxa are not overrepresented in any statistical analyses. Finally, taxa that had a cumulative count of less than 10% across the remaining samples were removed, preventing statistical anomalies, and decluttering the dataset. This resulted in the removal of 43 species. Without this data processing stage, the statistical noise and variability within the data set was too high to reveal meaningful patterns.
5. Results and discussion
5.1. Rollrock Section
5.1.1. Sample clusters
In total, 200 samples were processed and analysed from the Rollrock Section. Recovery of marine palynomorphs varies within the formations, but the highest recovery comes from the lower Deer Bay Formation below the intra-Berriasian unconformity. Important dinoflagellate cysts are illustrated in Fig. 2. A detailed zonal scheme is presented in Ingrams et al. (Reference Ingrams, Jolley and Schneider2021).
Using the methodology outlined above, 187 samples and 93 taxa were analysed across the three formations of the Rollrock Section. Q-mode cluster analysis delineated three clusters and six sub-clusters (Fig. 3h), which correspond to the stratigraphic log of the Rollrock Section (Figs 3b, 2e). These clusters display strong stratigraphic control. The Ringnes Formation entirely comprises alternating local assemblage zones of clusters 1a and 1b. The Isachsen Formation contained one sample, placed into cluster 3a.
Statistical data generated by marine palynomorphs of the Rollrock Section. (a) Lithology. (b) Cluster association. (c) Formations. (d) Sequences. (e) Sub-cluster association. (f) Local assemblage zones. (g) Dominant process type. (h) Q mode cluster dendrogram.
The Deer Bay Formation (250.5 m–522 m, Fig. 3c) contains all six sub-clusters but can be separated into three local assemblage zones (LAZs) based on distinct cluster assemblages (Fig. 3f). These LAZs occur as a result of shifts to new dinoflagellate cyst morphologies (Fig. 3f, g). Samples that delineate into the non-dominant cluster display reduced numbers of the dominant morphology. In Zone 1 the sample at 363 m delineating into cluster 2b coincides with a macrofossil horizon (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), a transgressive surface, and the first occurrence of the chorate species Oligosphaeridium complex (Ingrams et al. Reference Ingrams, Jolley and Schneider2021).
The base of LAZ 2 marks a horizon over which all data sets abruptly change, a common factor in other statistical analyses used on this interval. This is reflected in a dramatic increase of proximochorate cysts, from approximately 20% below this horizon, to approximately 50% above. Geochemical analysis also identifies this horizon, evidenced by sizeable increases in all detrital proxies analysed by PXRF (Appendix 2). Palynological evidence dates this horizon as Berriasian (Ingrams et al. Reference Ingrams, Jolley and Schneider2021), the intra-Berriasian unconformity marking a hiatus within the Sverdrup Basin (Kemper Reference Kemper1975). The evidence presented here confirms that this unconformity occurs, and that it does not equate to the Jurassic–Cretaceous boundary.
5.1.2. Microplankton groups
From DCA of the dinoflagellate cyst taxa found within the Rollrock Section (Fig. 4) five distinct groups were identified. These DCA groups each reflect closely associated taxa whose distribution was controlled by similar environmental factors. These groups are correlative with stratigraphic distributions of the previously delineated clusters (Fig. 5; for a results summary see Table 1). Higher values along axis 1 commonly correlate to taxa found more abundantly in younger samples, indicating a strong stratigraphical control over the data set.
Detrended correspondence analysis bi-plot output showing taxa ordinated in a two-dimensional plane. Convex hulls embrace associated groups of taxa. Taxa outside the hulls are not associated with any of the groups.
Summary of stratigraphical and statistically important taxa influencing detrended correspondence analysis groups linked to cluster association and stratigraphical occurrence.
The scale on axis 1 represents the standard deviation (SD) of taxon turnover. A taxon is expected to appear, rise to its mode, and disappear within four SD units (Hill & Gauch Reference Hill and Gauch1980). This implies that taxa which are more than four SD units apart on axis 1 should have no overlap. Generally, a change of approximately 50% in sample assemblage composition should occur within one SD unit (Hill & Gauch Reference Hill and Gauch1980).
Data from the DCA plot of the Rollrock Section are affected by variables represented by the first two axes, which possess eigenvalues of 0.37 (axis 1) and 0.15 (axis 2). Chorate taxa plot with high values on axis 1, while proximochorate taxa plot with high values on axis 1 and low values on axis 2. Gonyaulacysta species plot with low axis 1 values. Therefore, it is possible that axis 1 represents nutrient availability or turbidity.
5.1.3. Palaeoenvironmental analysis
In order to determine what the palynological and statistical trends are reflecting, a link needs to be established to a controlling environmental factor. CCA of palynological and elemental data has previously been used to delineate controlling environmental factors (e.g., Hammer & Harper, Reference Hammer and Harper2006). In this study, this method has been applied to the taxonomic groups previously identified by cluster and DCA analysis (Fig. 6). A positive relationship between the aluminium/silica (Al/Si) ratio and cluster 3 was observed, and a negative relationship with clusters 1 and 2a (Figs 3h, 6). The rubidium/strontium (Rb/Sr) ratio shows a weak positive relationship with cluster 2b. The zirconium/rubidium (Zr/Rb) ratio displays an inverse trend to that of Al/Si, with a negative relationship with cluster 3 and a positive relationship with clusters 1 and 2a.
Canonical correspondence analysis displaying environmental controls over sample cluster association and detrended correspondence analysis taxa groupings.
The Rb/Sr is a strong proxy for weathering and coastline proximity. When this ratio is high, the sediment is identifiably more immature. Rubidium is a highly leachable element; thus, its presence in increased amounts indicates that the source sediment is originating from an area exposed to a high degree of weathering leading to higher nutrient levels within the sediment load. Zr/Rb is an indicator of low nutrient levels, and therefore, indicates the opposite to Rb/Sr. Zr/Rb is also used to track changes in sediment grain size (Calvert & Pedersen, Reference Calvert and Pedersen2007), as Zr often resides in coarser grained particles than Rb. Al/Si is a reliable indicator of clay content in the sediment. High Al/Si values are associated with lower energy, deeper water environments, where Al is an indicator of the clay component of the sediment load and Si is an indicator of coarser grained material. Because all samples were taken from roughly similar fine-grained lithology, it is inferred herein that samples with lower values of this ratio are siltier than those with a higher ratio.
While CCA is strongly influenced by stratigraphy, some conclusions can still be drawn. There is a clear divide between samples from above and below the aforementioned intra-Berriasian unconformity (Fig. 6). Sediments generally control nutrient availability, and those deposited above the unconformity are much more clay rich, and as such indicate a lower energy, more nutrient depleted environment.
5.2. Post intra-Berriasian unconformity
5.2.1. Sample clusters
In order to remove the stratigraphic controls present in the data, the Deer Bay Formation above the unconformity has been examined separately, with samples taken systematically every 1.5 m. Using the methodology outlined in the previous sections, the upper Deer Bay Formation and a singular sample from the Isachsen Formation were analysed using Q-mode cluster analysis resulting in four clusters being delineated (Fig. 7d).
(a) Lithology. (b) Cluster association. (c) Zones. (d) Cluster dendrogram of the upper Deer Bay Formation.
When comparing these clusters to the lithostratigraphy of the Rollrock Section four clear zones are observed (Fig. 7c). Cluster uDB3, delineated from the upper Deer Bay Formation, is directly linked to cluster 2b from the whole section analysis. Consequently, this cluster/sub-cluster is confirmed to be controlled by an external environmental factor rather than by chronological changes. Clusters uDB1, uDB2 and uDB4 (Fig. 7d) are correlated to cluster 3 from the whole section analysis (Fig. 3h), adding further emphasis to the strong stratigraphical control of the whole section. On the other hand, this result confirms that clusters delineated during separate analysis of the upper Deer Bay Formation are controlled by non-chronological factors.
5.2.2. Microplankton groups
The taxa present in the upper Deer Bay Formation were subjected to a separate DCA (Fig. 8). Using the methodology detailed above, a further 23 taxa were discarded, resulting in 69 taxa being analysed across the 88 viable samples of the upper Deer Bay Formation. The eigenvalues of axis 1 and axis 2 (0.25 and 0.13, respectively) show a positive correlation between samples and taxa. Cumulative percentages show that axis 1 accounts for twice the amount of variance of axis 2. While the eigenvalues might appear low, count data, even after filtering, is inherently noisy, and these values are typical when dealing with palynomorph data sets that have a high number of variables (Daly et al. Reference Daly, Jolley, Spicer and Ahlberg2011).
Detrended correspondence analysis bi-plot of taxa recovered from the upper Deer Bay Formation. Shaded areas indicate close taxa association.
From DCA of this part of the section it is possible to identify four groups of taxa and four outlying taxa (Fig. 8). The four groups vary in distribution and abundance (Table 2; Fig. 9). Plotting the distributions of these groups highlights trends that are not apparent from analysis of the entire section.
Summary of linkage of detrended correspondence analysis groups from the upper Deer Bay Formation with cluster analysis and stratigraphical occurrence.
Group uDBIV contains many poorly preserved proximate taxa that do not directly correspond to the delineated clusters. The taxa in this group, such as Pareodinia borealis and Pareodinia ceratophora are present in the majority of samples, and as such can be considered to be the dominant autotrophic population of the section. These taxa remain largely unaffected by environmental controls exerted on the section. A similar pattern is observable in group uDBII.
The taxa grouped within uDBIII (Table 2) are episodically common in this part of the section (Fig. 9). Where uDBIII becomes the most abundant group, samples delineate into cluster uDB3. Where uDBIII is not the most abundant group and numbers of taxa found within group uDBII are low (Table 2), samples delineate into cluster uDB4 (Fig. 9). In the whole section analysis, the uDBII pattern is overprinted by the presence of chorate species of the genus Oligosphaeridium, which are almost entirely absent in the section below the unconformity.
5.2.3. Palaeoenvironmental analysis
To reveal links between sample clusters, DCA taxa groups and environmental factors, CCA was undertaken using PXRF element ratios as environmental proxies. Three types of positive relationships were recovered (Fig. 10).
Canonical correspondence analysis displaying environmental controls over sample cluster association and detrended correspondence analysis taxa groupings taken from the upper Deer Bay Formation.
A close association of uDB1 and uDB2 is observed (Fig. 10) as their palynofloral composition is similar (Fig. 7d). uDB2 has a slightly stronger positive relationship with Al/Si indicating deposition in more clay rich conditions. Because all the samples are taken from roughly the same lithology and Zr/Rb, as a proxy of grain size, has only a weak relationship with uDB4, it is clear that another factor must also be controlling distribution. However, the uDB4 group contains many samples where preservation is of a significantly lower standard. Likewise, many of the palynomorphs found in these groups are degraded and are only identifiable to genus level. Therefore, it is possible that the change in grain size has affected preservation, causing degradation of palynomorphs either during or after deposition.
5.3. Sequence stratigraphic analysis
5.3.1. Third order sequences
The Rollrock Section is contained within the mid Permian–Hauterivian first order sequence and the Oxfordian–Hauterivian second order sequence sensu Embry (Reference Embry1993) and Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019). The multidisciplinary approach outlined above, combining sedimentology, palynology and geochemistry, has revealed five third order sequence stratigraphic cycles in the mudstone-dominated Rollrock Section (Fig. 11), which are compared to the sequences identified by Embry (Reference Embry1993) and Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) (Table 3).
Stratigraphic distribution of values of dominance, Shannon-H diversity and detrended correspondence analysis Axis 1, calculated for marine palynomorphs.
Third order sequence stratigraphic packages identified in this study with an age comparison to those identified by Embry (Reference Embry1993) and Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019).
Two key sequence stratigraphic surfaces, that is, sequence boundaries (SBs) and maximum flooding surfaces (MFSs), can generally be identified using marine palynology. Generally, SBs are represented by a relative loss in dinoflagellate cyst abundance and diversity. In contrast, MFSs are represented by the highest relative abundance and diversity of dinoflagellate cysts, resulting from the expansion of habitats associated with transgressions and a reduction in relative energy levels, allowing for a more complete plankton (Morley, Reference Morley1996). The Rollrock Section displays varying dinoflagellate cyst abundance patterns, which are used herein as the main palynological indicator for identifying sequences.
In a shelf environment, cyst bearing dinoflagellates bloom with greater diversity in relatively deep and less turbulent waters (e.g., Posamentier et al. Reference Posamentier, Jeniey, Vail, Wilgus, Hastings, Kendall, Posamentier, Ross and van Wagoner1988; Wornardt, Reference Wornardt1993; Armentrout, Reference Armentrout1996; Morley, Reference Morley1996). In contrast, assemblages in turbulent or stressed environments are often dominated by a few species (e.g., Armentrout, Reference Armentrout1996). Utilising a combination of dinoflagellate cyst diversity and sedimentology, a sequence stratigraphic framework has been defined for the Rollrock Section, comprising three complete and two incomplete sequences (Table 3).
Sequence 1 (0 m–141 m): Sequence 1 is characterised by sparse data and dinoflagellate cysts are often highly degraded, resulting from both depositional and diagenetic processes. Sequence 1 covers the lower portion of the logged Ringnes Formation. The top of sequence 1 is defined by a 2 m thick fine grained sandstone unit at 141 m (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). Within sequence 1, dinoflagellate cyst diversity is very low from 22.5 m–61.5 m, but this is partially caused by poor preservation and recovery. An approximate 20 m cyclicity in dinoflagellate cyst diversity is observable between 61.5 m and the SB. Whether this represents fourth order cyclicity is undetermined. The base of sequence 1 lies within the Oxfordian, with the first identifiable Kimmeridgian level at 132 m (Ingrams et al. Reference Ingrams, Jolley and Schneider2021). With regard to age, this sequence correlates with sequence 8 of Embry (Reference Embry1993) and with the bottom half of the base Oxfordian sequence of Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) (Table 3). All samples taken from this sequence plot entirely within cluster 1 (Fig. 3b).
Sequence 2 (141 m–230 m): Sequence 2 is composed of mudstones of the upper Ringnes Formation. The upper SB is defined as the base of the first very fine-grained sandstone unit with large concretions (230 m, Fig. 3), which marks the upper part of the Ringnes Formation (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). Dinoflagellate cyst diversity changes cyclically within an overall increasing trend to 196.5 m. This level contains the highest dinoflagellate cyst diversity, corresponds to the second of three macrofossil horizons containing Buchia rugosa (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), and is identified as the MFS (Fig. 11). The cycles below the MFS are on average 15 m thick and relatively consistent and could be argued to represent fourth order sequence cycles. However, due to the lack of more detailed evidence, they are not identified as such within this study. Above the MFS, dinoflagellate cyst diversity trends cyclically downwards towards the SB. The youngest diversity peak occurs 9.5 m above the MFS and 14 m below the SB. Ingrams et al. (Reference Ingrams, Jolley and Schneider2021) determined the age of this sequence as middle Kimmeridgian–late Tithonian. Schneider et al. (Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020) assigned the B. rugosa horizons at 192, 196.5, and 196.8 m to the early Tithonian B. rugosa zone. This sequence correlates with sequence 9 of Embry (Reference Embry1993) and the upper half of the base Oxfordian sequence of Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) (Table 3). The MFS of this sequenced was hypothesised by Embry (Reference Embry1993) to be close to the Kimmeridgian–Tithonian boundary based on evidence from Buchia bivalves reported by Balkwill (Reference Balkwill1983). The samples taken from this sequence mostly delineate into cluster 1, with four samples delineating into cluster 2 (Fig. 3h).
Sequence 3 (230 m–379.5 m): Sequence 3 comprises siltstones and very-fine grained sandstones from the upper Ringnes Formation and the lower mudstones of the Deer Bay Formation. The SB is located at 379.5 m at a thin, well indurated siltstone bed (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), which corresponds with the intra-Berriasian unconformity. Dinoflagellate cyst diversity increases cyclically up to 292.5 m and decreases cyclically above until the SB (Fig. 11). These cycles are on average 12.5 m thick (10.5 m–17.5 m), potentially reflecting fourth order sequences. Sequence 3 was dated as Tithonian–Berriasian by Ingrams et al. (Reference Ingrams, Jolley and Schneider2021). Several macrofossil horizons occur within the regressive systems tract of this sequence, containing ammonites and Buchia bivalves described in detail in Schneider et al. (Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020), which confirm the Tithonian–Berriasian age. This sequence correlates with sequence 10 of Embry (Reference Embry1993) and the base Tithonian sequence of Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) (Table 3).
Recent finds of Borealites fedorovi, Buchia okensis and O. complex indicate an (early) Berriasian age below the sequence boundary at the unconformity, correlating with the age proposed by Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019). The MFS for the sequence described by Embry (Reference Embry1993) occurs close to the base of the sequence, creating a large regressive systems tract. The MFS in the present study is also seen to be near the base of the sequence creating a large highstand systems tract. The samples in this sequence mostly delineate into cluster 1 below the MFS and into cluster 2 above, although there are exceptions in both parts of the sequence (Fig. 3b). The samples collected from the lowstand systems tract (230 m–251 m) all delineate into cluster 1 (Fig. 3b).
Sequence 4 (379.5 m–524.5 m): Sequence 4 comprises mudstones in the upper Deer Bay Formation. The SB is located at the base of the Isachsen Formation (524.5 m). Like in the preceding two sequences, dinoflagellate cyst diversity trends cyclically upwards until it reaches the MFS (411 m), before cyclically trending downwards towards the SB (Fig. 11). Sequence 4 was dated as late Berriasian–Valanginian based on palynology (Ingrams et al. Reference Ingrams, Jolley and Schneider2021) and as broadly Valanginian based on sparse macrofauna (Schneider et al. Reference Schneider, Kelly, Mutterlose, Herrle, Hülse, Jolley, Schröder-Adams and Lopez-Mir2020). This sequence roughly correlates with an unnamed third order sequence of Embry (Reference Embry1993) that incorporates the Berriasian and terminates at the top of the Awingak Formation. However, the Awingak Formation does not occur in the more distal Rollrock Section. The samples from this sequence delineate into cluster 2b below 405 m and mostly into cluster 3 above. Unlike for previous sequences, there is a greater degree of variation in dinoflagellate cyst diversity in this sequence, and a more detailed analysis was undertaken (Fig. 12).
Stratigraphic distribution of detrended correspondence analysis taxa groups of the upper Deer Bay Formation identified in Figure 8. Green bands represent fourth order regressive systems tracts, blue bands represent fourth order transgressive systems tracts, the yellow band represents a third order lowstand systems tract.
Embry (Reference Embry1993) hypothesised that the Upper Jurassic to Lower Cretaceous sedimentary succession of the Sverdrup Basin can be assigned to six third order sequence stratigraphic cycles. The oldest three cycles range from the Oxfordian to the early Kimmeridgian, the late Kimmeridgian to the early Tithonian, and the late Tithonian to the Jurassic–Cretaceous boundary. The three Cretaceous sequences were not dated. However, the upper boundary of the sixth third order sequence is the sub-Hauterivian unconformity, positioned within the Isachsen Formation, but stratigraphically above the succession studied herein (see also Galloway et al. Reference Galloway, Tullius, Evenchick, Swindles, Hadlari and Embry2015). This concept was updated by Embry (Reference Embry2011), Embry & Beauchamp (Reference Embry, Beauchamp and Miall2019) and Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) who divided the Upper Jurassic to lowermost Cretaceous succession into three third order cycles: base Oxfordian to base Tithonian; base Tithonian to mid-Berriasian/Valanginian; and mid-Berriasian/Valanginian to Hauterivian. The poorly resolved boundary age of the second and third cycles indicates that this level was taken at the intra-Berriasian unconformity.
The discrepancy in the number of third order sequences can be attributed to the methodology used to identify sequences. Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) used transgressive–regressive (T-R) sequences to determine boundaries, where the maximum regression surface (MRS) is taken as the sequence boundary. This enables the discovery of tectonically generated, large magnitude SBs with associated unconformities. The present study utilises a different sequence stratigraphic terminology, where a sequence is defined by correlative conformities (e.g., Van Wagoner, Reference van Wagoner, Posamentier, Mitchum, Vail, Sarg, Loutit, Hardenbol, Wilgus, Hastings, Kendall, Posamentier, Ross and Van Wagoner1988; Nichols, Reference Nichols2009), expressed in the Rollrock Section as sandstone bodies. The difference between the two approaches becomes most obvious when comparing the top of the sequence that begins at the post-Berriasian unconformity. Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) place the top of this sequence at the sub-Hauterivian MRS. Herein, the upper boundary is placed at the inception of the Isachsen Formation, and the Valanginian part of the Isachsen Formation conforms to an additional third order sequence.
Embry et al. (Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019) identified a third order sequence from the base Oxfordian to the base Tithonian (Table 3). Both this study and Embry (Reference Embry1993) split this sequence into two different sequences (Table 3). The boundary between these two sequences does not meet the criteria of a large-magnitude boundary generated by tectonically driven base level changes rather than by eustasy (Embry et al. Reference Embry, Beauchamp, Dewing, Dixon, Piepjohn, Strauss, Reinhardt and McClelland2019). Therefore, the sequence boundary between sequences 1 and 2 in the Rollrock Section is controlled by eustacy rather than tectonic activity.
5.3.2. Fourth order sequences, upper Deer Bay Formation
Applying the methodology outlined above, dinoflagellate cyst diversity and sedimentology have been used to determine ten fourth order sequences (Table 4). Fourth order low stand systems tracts are unidentifiable since the upper Deer Bay Formation is entirely composed of mudstone and siltstone. Consequently, the data were studied as a T-R system. Sequence boundaries and transgressive surfaces were identified by changes in the diversity curve, the former being identified by minimum diversity and the latter by maximum diversity (Morley, Reference Morley1996).
Intervals, thicknesses and transgressive surfaces of fourth order sequence stratigraphic cycles identified in the upper Deer Bay Formation.
By comparing these fourth order sequences with the distribution of taxa within DCA groups uDBI–uDBIV several patterns are observable (Fig. 12). There is a clear separation of taxa occurring in transgressive and regressive periods.
The DCA group IV/uDBIII dominates the section from the third order SB up to 405 m. While the group is present throughout sequence 4, it cyclically declines (Fig. 12), being most abundant in the third order transgressive systems tract immediately above the unconformity. Moreover, this group is seen to increase in abundance above transgressive surfaces, during regressive periods. Group uDBIII is composed primarily of proximochorate cysts (e.g., Trichodinium erinaceoides and Gochteodinia virgula), which display a strong positive relationship to uDB3 (Fig. 7d) and fourth order highstand systems tracts (Fig. 12), Rb/Sr (Fig. 10). The break in sedimentation, associated with the unconformity, and the increase of proximochorate species making up uDBIII, suggest that these taxa outcompete other species during periods of lower relative sea level.
Similarly, the abundance of group uDBII increases above transgressive surfaces. However, uDBII displays reduced abundances near the bottom of the sequence, where the respective taxa were outcompeted by those in uDBIII (Fig. 12). In contrast, group uDBII displays an increase in abundance towards the top of sequence 4, because the final two fourth order sequences were generally shallower than those that preceded them. Within this interval, nutrient flux was different from that in the basal part of sequence 4, and no group uDBIII was established (Fig. 10).
While group uDBIV has the same stratigraphical pattern as group uDBII, a different conclusion can be drawn. uDBIV displays generally higher abundances of taxa than uDBII and contains taxa that are present in relatively stable numbers throughout the upper Deer Bay Formation. This suggests that they maintained stable populations, while, at the same time, variations in the abundance of the other groups provide evidence of changes in palaeoecology.
Group uDBI occurred in higher frequencies below transgressive surfaces, during transgressive periods, but is poorly represented in the first two fourth order sequences. This pattern suggests that species in this group outcompeted other taxa during periods of relatively high sea level. There are some anomalies, for example, at 430.5 m, where the abundance of group uDBI decreased within a transgressive systems tract. However, in the latter sample this decrease is primarily down to poor preservation rather than ecological control. Group uDBI, composed primarily of chorate cysts such as O. complex, displays strong positive relationships to fourth order transgressive tracts (Fig. 12), Al/Si values (Fig. 10) and to uDB1 and uDB2 (Fig. 7d).
From these data, DCA axis 1 (Fig. 8) is interpreted to reflect nutrient availability and/or water depth. The proximochorate dominated uDBIII group is a proxy for more proximal, high energy, nutrient rich conditions, while the chorate dominated uDBI group is a proxy for distal, low energy, reduced nutrient conditions. These two groups show a departure from normal conditions, represented by groups uDBII and uDBIV, and as such are only proxies relative to the original state. Group uDBI is interpreted to reflect deeper and calmer water masses. Group uDBIII in contrast reflects shallower and more turbid environments.
5.4. Microplankton paleobiology
Dinoflagellates, like all other organisms, have evolved to meet the conditions of specific habitats. The evidence presented here shows two main morphological adaptations that benefit organisms in specific environments. Taxa possessing chorate processes are observed to dominate relatively deeper calmer, conditions, while taxa possessing proximochorate processes are observed to dominate relatively shallower, more turbid conditions.
Long processes on chorate cysts are associated with deeper-water, lower-energy, warmer conditions (e.g., Poulsen & Riding, Reference Poulsen and Riding2003; Carvalho et al. Reference Carvalho, Bengtson and Lana2016). Processes have been hypothesised to be floatation devices that are a necessary adaptation in warmer waters (Lentin & Williams Reference Lentin and Williams1980), because the specific gravity of water falls at higher temperatures (Poulsen & Riding Reference Poulsen and Riding2003), as molecules gain more energy and expand. In modern samples, process length has been directly correlated to salinity and sea surface temperatures (e.g., Mertens et al. Reference Mertens, Ribeiro, Bouimetarhan, Caner, Nebout, Dale, De Vernal, Ellegaard, Filipova, Godhe and Goubert2009, Reference Mertens, Bradley, Takano, Mudie, Marret, Aksu, Hiscott, Verleye, Mousing, Smyrnova and Bagheri2012a, Reference Mertens, Bringué, Van Nieuwenhove, Takano, Pospelova, Rochon, De Vernal, Radi, Dale, Patterson and Weckström2012b). While it is possible that this method could be applied to different genera in the Mesozoic, analysis of the data collected from the Rollrock Section indicate it cannot be directly applied to this study. The palynomorphs recovered from the Rollrock Section have been diagenetically altered and as such display high amounts of intraspecific variation. For example, processes of O. complex were measured from two samples (456.0 m and 463.5 m; a fourth order transgressive surface and sequence boundary, respectively) from specimens with low amount of visible alteration. However, no meaningful data were recovered, with process lengths ranging from 19 μm to 33 μm. Variation within a single specimen can range between 3 μm and 9 μm, and no discernible difference in average process length between the two samples was observed.
Oligotrophic, warmer, and deeper habitats in modern oceans are observed to be dominated by nutrient stress tolerant taxa (Smayda & Reynolds Reference Smayda and Reynolds2003). These are typically very large, slow growing and often highly ornamented species (Smayda & Reynolds Reference Smayda and Reynolds2003). In this study, species of Oligosphaeridium are interpreted to have dominated assemblages in similar habitats.
In previous studies of dinoflagellate cysts from the Sverdrup Basin, frequency increases in small spinose cysts during several intervals throughout the Jurassic and Cretaceous were identified (Pocock Reference Pocock1976; Ingrams et al. Reference Ingrams, Jolley and Schneider2021). These cysts were never formally identified by Pocock (Reference Pocock1976), but instead were described as ovoid with definite polarity. This lead Davies (Reference Davies1983) to hypothesise that these cysts either represented Exochosphaeridium scitulum or T. erinaceoides both of which are present in the Rollrock Section (Ingrams et al. Reference Ingrams, Jolley and Schneider2021). T. erinaceoides peaks in frequency within three intervals in the Rollrock Section (306.0–312.0 m, 363.0–364.5 m, and 379.5–405.0 m). Species of the genus Exochosphaeridium have previously been associated with nearshore, high-energy conditions (Li & Habib Reference Li and Habib1996; Lamolda & Mao Reference Lamolda and Mao1999; Harris & Tocher Reference Harris and Tocher2003; Barroso-Barcenilla et al. Reference Barroso-Barcenilla, Pascual, Peyrot and Rodríguez-Lázaro2011; Peyrot et al. Reference Peyrot, Barroso-Barcenilla, Barrón and Comas-Rengifo2011; van Helmond et al. Reference van Helmond, Sluijs, Damsté, Reichart, Voigt, Erbacher, Pross and Brinkhuis2014; Carvalho et al. Reference Carvalho, Bengtson and Lana2016).
Species distribution within modern dinoflagellate communities is primarily dependent on a combination of physical and chemical parameters, including turbulence, solar irradiance and nutrient levels (Smayda & Reynolds Reference Smayda and Reynolds2003). Shallow-water and seasonal-bloom species are characteristically small with a high surface area to volume ratio (Smayda & Reynolds Reference Smayda and Reynolds2003). While this does not necessarily influence the morphological characteristics of a cyst, it is notable. For a dinoflagellate, the easiest way to obtain a higher cyst surface area to volume ratio is to produce numerous short spines. This higher surface area to volume ratio prevents cysts from excess movement in high-energy conditions, thereby preventing damage to the theca inside.
6. Summary
A multivariate statistical analysis of the marine palynomorphs recovered from the Late Jurassic to earliest Cretaceous interval of the Rollrock Section, Arctic Canada, allowed for the identification of three clusters and six sub-clusters, each with their own unique floral assemblage. These clusters reflect discrete chronological periods and ecological conditions, which correspond to the stratigraphy of the section. The Oxfordian to Tithonian Ringnes Formation is recorded as being dominated by cluster 1, an assemblage comprising proximate dinoflagellate cysts. The Tithonian to Valanginian Deer Bay Formation is divided by an intra-Berriasian unconformity and is separated into three local assemblage zones based on dinoflagellate cysts with distinct process morphologies. Proximate cysts (cluster 2a) dominate in the Tithonian to lower Berriasian, proximochorate cysts (cluster 2b) in the upper Berriasian, and chorate cysts (cluster 3) in the Valanginian.
Statistical palynological data, combined with sedimentological evidence, subdivides the Rollrock Section into three complete and two incomplete third order stratigraphic sequences. By combining dense and systematic sampling with the analysis of changes in dinoflagellate cyst diversity, distinct fourth order sequences have been recorded across the Jurassic–Cretaceous transition within the Sverdrup Basin for the first time. By analysing multivariate data through this sequence stratigraphic framework, a more complicated environmental transition is observed than previously suggested for the basin, as palynological assemblages are driven by these fourth order cycles.
In the Sverdrup Basin, two groups of dinoflagellate cysts, characterised by process morphology, are observed to act as environmental proxies that depart from normal conditions. This is evident within fourth order sequences, with proximochorate genera, such as Lanterna and Gochteodinia, and proximate genera, such as Pareodinia, being prevalent during transgressive systems tracts. In contrast, chorate species, such as O. complex and Oligosphaeridium asterigium, are prevalent during highstands.
The ratio of Rb/Sr, used as a proxy for weathering, coastline proximity, and chemical leaching, is observed to have a direct correlation to palynoassemblage constitution. Elevated Rb/Sr ratios are interpreted to correspond to high-energy, turbid, proximal, and nutrient-rich conditions. These conditions selected for high frequencies of proximochorate cyst bearing dinoflagellates, which were able to outcompete dinoflagellates with other cyst types in regressional tracts.
The ratio of Al/Si is a reliable indicator of clay content in samples, which in turn can be utilised as a proxy for hydrodynamic energy, shoreline proximity, and nutrient availability. A high ratio indicates lower energy, a distal setting and decreased nutrient content, while a low ratio indicates the opposite. In the Rollrock Section, this ratio has a positive correlation with the abundance of chorate cysts; high values of both categories correspond to fourth order transgressional systems tracts.
Integration of these newly discovered fourth order sequences into future palaeoclimate studies, within the Sverdrup Basin and the wider Arctic region, will enable more accurate data to be obtained. Sparse sampling of sections across the Jurassic–Cretaceous transition, which bypasses identification of these cycles, inevitably leads to oversimplifying the environmental perturbations that characterise this interval.
7. Supplementary material
Supplementary material is available online at https://doi.org/10.1017/S1755691022000081.
8. Acknowledgements
The authors thank the following people and institutions for their valuable support: Sylvie LeBlanc (Department of Culture and Heritage, Iglooik, Canada); Jane Chisholm and rangers of Parks Canada (Iqaluit and Tanquary Camp, Canada); John Innis (Universal Helicopters); and the staff of Polar Continental Shelf Programme at Resolute Bay (Canada). Fellow geologists Berta Lopez-Mir and Peter Hülse (both Cambridge Arctic Shelf Programme (CASP), Cambridge, UK) participated in fieldwork in 2015. The help of field assistant Alex Chavanne (California, USA) with logging and sampling the Rollrock Section was instrumental. Dave Bodman of MB Stratigraphy Ltd. (Sheffield, UK) prepared part of the palynological slides used in this study. CASP's industry sponsors are acknowledged for their funding of the Canadian Arctic Islands Project. The authors also thank reviewers James Riding (British Geological Survey, Nottingham, UK) and an unknown second reviewer, for their constructive criticism of this paper and the Earth and Environmental Science Transactions of the Royal Society of Edinburgh editorial office.
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