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Latitudinal influences on bryozoan calcification through the Paleozoic

Published online by Cambridge University Press:  02 September 2022

Catherine M. Reid Open the ORCID record for Catherine M. Reid [Opens in a new window] ,
Patrick N. Wyse Jackson  and
Marcus M. Key Jr.
Catherine M. Reid*
Affiliation:
School of Earth and Environment, University of Canterbury, Christchurch 8140, New Zealand. E-mail: [email protected]
Patrick N. Wyse Jackson
Affiliation:
Department of Geology, Trinity College, Dublin 2, Ireland. E-mail: [email protected]
Marcus M. Key Jr.
Affiliation:
Department of Earth Sciences, Dickinson College, Carlisle, Pennsylvania 17013-2896, U.S.A. E-mail: [email protected]
*
*Corresponding author.
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Abstract

Bryozoans are active non-phototrophic biomineralizers that precipitate their calcareous skeletons in seawater. Carbonate saturation states varied temporally and spatially in Paleozoic oceans, and we used the Bryozoan Skeletal Index (BSI) to investigate whether bryozoan calcification was controlled by seawater chemistry in Paleozoic trepostome and cryptostome bryozoans. Our results show that cryptostome bryozoan genera were influenced by ocean chemistry throughout the Paleozoic and precipitated the most calcite at lower latitudes, where carbonate saturation states are generally higher, and less in midlatitudes, where carbonate will be relatively undersaturated. Trepostome bryozoan genera show a similar but weaker trend for the Ordovician to Devonian, suggesting that, like the cryptostomes, they were unable to metabolically overcome falling saturation states and simply precipitated less robust skeletons at higher latitudes. Carboniferous to Triassic trepostomes differ, however, and show a trend toward increased calcification at higher latitudes, indicating an ability to overcome unfavorable carbonate saturation states. Analysis of Permian trepostomes at the species level indicates this is most pronounced in the Southern Hemisphere, where calcification is matched by increased feeding capacity. It is proposed that this increased feeding capacity allowed trepostomes to metabolically overcome unfavorable carbonate saturation states. The differing responses of trepostome and cryptostome bryozoans to carbonate saturation states suggest that bryozoans should not be considered as a single group in marine extinctions linked to ocean chemistry changes. Likewise, it would suggest that modern stenolaemate and gymnolaemate bryozoans should be treated separately when considering their response to modern ocean chemistry changes.

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Paleobiology , Volume 49 , Issue 2 , May 2023 , pp. 271 - 283
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This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (https://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution, and reproduction in any medium, provided the original work is properly cited.
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Copyright © The Author(s), 2022. Published by Cambridge University Press on behalf of The Paleontological Society

Introduction

Marine bryozoans are calcified colonial suspension-feeding invertebrates and have an extensive fossil record through the Paleozoic in both warm and cold marine waters (Taylor and Allison Reference Taylor and Allison1998). The first records of non-calcified bryozoans are now known from the Cambrian (Zhang et al. Reference Zhang, Zhang, Ma, Taylor, Strotz, Jacquet, Skovsted, Chen, Han and Brock2021), and all Paleozoic stenolaemate orders (Cryptostomata, Cyclostomata, Cystoporata, Estonioporata, Fenestrata, and Trepostomata) were established by the Early Ordovician (Ma et al. Reference Ma, Buttler, Taylor, Rosso, Wyse Jackson and Porter2014). Almost all Paleozoic stenolaemate bryozoans disappeared during the end-Paleozoic extinction, with the trepostomes and cystoporates persisting until the Late Triassic (McKinney and Jackson Reference McKinney and Jackson1991). The cyclostomes were relatively sparse in the Paleozoic but are the only Paleozoic stenolaemate order to survive to the Recent. The gymnolaemate Cheilostomata that dominate modern oceans only appeared in the Jurassic (Taylor Reference Taylor1994).

Bryozoans, like other marine invertebrates with calcareous hard parts, must precipitate their skeletons in seawater. Paleozoic stenolaemate bryozoans had calcitic skeletons (Taylor Reference Taylor2020) and are not known to have hosted photosymbionts (Key et al. Reference Key, Wyse Jackson, Hakansson, Patterson, Moore, Moyano, Cancino and Wyse Jackson2005). Many phylogenetically more primitive calcareous organisms, particularly phototrophic ones, are passive calcifiers, and they were influenced by changes in ocean chemistry through the Phanerozoic (Stanley and Hardie Reference Stanley and Hardie1998, Reference Stanley and Hardie1999), and bryozoans were initially proposed to be among this passive calcifying group. Paleozoic bryozoans are now known to be active biomineralizers (Taylor and Kuklinski Reference Taylor and Kuklinski2011; Key et al. Reference Key, Wyse Jackson and Reid2022) rather than passive calcifiers and show no response to secular changes in ocean calcite-aragonite chemistry. Bryozoans, however, must still accommodate biomineralization issues associated with pCO2 fluctuations and temperature-controlled changes in marine carbonate saturation state and the availability of skeleton-building ions (James and Jones Reference James and Jones2015). Modern bryozoan growth rates are usually higher during warmer months in areas with higher seasonal temperature variation (Lombardi et al. Reference Lombardi, Cocito, Occhipinti-Ambrogi and Hiscock2006), and some produce distinct growth checks in colder months (e.g., Patzgold et al. Reference Patzgold, Ristedt and Wefer1987; Barnes Reference Barnes1995; Key et al. Reference Key, Rossi, Smith, Hageman and Patterson2018) linked to seasonal food availability (Brey et al. Reference Brey, Gutt, Mackensen and Starmans1998; Smith Reference Smith2007). Cenozoic gymnolaemate bryozoans may have calcite, aragonite or bimineralic skeletons, and the occurrence of aragonite and bimineralic forms increases markedly toward the tropics (Taylor et al. Reference Taylor, James, Bone, Kuklinski and Kyser2009). Additionally, in modern bimineralic bryozoans, the proportion of calcite to aragonite skeleton precipitated by the zooid varies seasonally (Lombardi et al. Reference Lombardi, Cocito, Hiscock, Occhipinti-Ambrogi, Setti and Taylor2008), indicating bryozoans are responding to saturation states. Therefore, it might be expected that Paleozoic bryozoans should have larger or more robust skeletons in warmer lower-latitude waters and would be smaller or less robust in colder water at higher latitudes in response to the decreased saturation state with increasing latitude. Following on from Taylor and Kuklinski's (Reference Taylor and Kuklinski2011) and Key et al.'s (Reference Key, Wyse Jackson and Reid2022) finding that bryozoans are active and not passive biomineralizers, this paper investigates the influence of paleolatitude on the calcification of selected Paleozoic stenolaemates (Trepostomata and Cryptostomata) and the potential difficulty of calcium carbonate precipitation in these bryozoans driven by oceanographic variation in carbonate saturation state. As carbonate saturation state cannot be directly measured from the fossil record, we use paleolatitude as a proxy.

Materials and Methods

The Bryozoan Skeletal Index (BSI) of Wyse Jackson et al. (Reference Wyse Jackson, Key, Reid, Wyse Jackson and Zagorsek2020) was used as proxy for the degree of calcification in bryozoans. Skeletal parameters gathered for trepostome and cryptostome colonies were mean autozooecial aperture diameter (MZD; mean diameter for circular apertures, and mean of minimum and maximum dimensions for oval apertures), exozone width (EW), and zooecial wall thickness in exozone (ZWT). The width of the zoarium (or thickness) (ZOW) was also recorded where available. The BSI measures the relative proportion of skeletal carbonate to intra-zoarial void space in stenolaemate bryozoan colonies (Fig. 1) and is calculated using the following equation:

(1)$${\rm BSI\ } = [ {( {{\rm EW\ } \times {\rm ZWT}} ) /{\rm MZD}} ] \times 100$$

Figure 1. Morphological characters used to derive the Bryozoan Skeletal Index (BSI) on a ramose zoarium. From Wyse Jackson et al. (Reference Wyse Jackson, Key, Reid, Wyse Jackson and Zagorsek2020: fig. 2). Abbreviations: EW, exozone width; MZD, autozooecial aperture diameter; ZWT, zooecial wall thickness.

The multiplication factor of ×100 ensures that BSI is a whole number. Higher numbers represent higher levels of calcification.

Data were gathered from the literature for all genera globally of the stenolaemate bryozoan orders Trepostomata and Cryptostomata from the Lower Ordovician to the Upper Triassic. Data were primarily gathered from original type species descriptions; however, where original descriptions did not include all required parameters, additional data were gathered from published works on the same species in the same location, unit, or age. Where possible, skeletal data were gathered from published data tables, but where numeric values were not available, we measured directly from published photomicrographs. For all species for which data were collected, relative age of the collection horizon was recorded and a numerical age derived from the updated International Commission of Stratigraphy chronostratigraphic chart (Cohen et al. Reference Cohen, Finney, Gibbard and Fan2013). Data were gathered for all colony morphologies; however, the BSI calculation strongly favors massive and encrusting forms that may have multilayered sheets. As cryptostomes have primarily ramose forms, only ramose forms were analyzed when comparing Ordovician to Triassic trepostome and cryptostome genera.

An additional dataset was gathered for 119 Permian trepostome bryozoan species to investigate the distribution of bryozoans from low to high paleolatitudes. Species recorded in more than one sedimentary basin were entered as data points for each basin where location-specific measurements were available. Where multiple colony morphologies were recorded, ramose colonies took precedence as the primary classification, followed in descending preference by encrusting, massive, and foliose colonies.

The same BSI parameters for all available trepostome bryozoan species were gathered from each depositional basin and were not restricted to type species occurrences. Permian Southern Hemisphere basins and locations included eastern Australia (Tasmania, Sydney, and Bowen Basins) (Crockford Reference Crockford1941, Reference Crockford1943, Reference Crockford1945; Wass Reference Wass1968; Reid Reference Reid2001, Reference Reid2003; Morozova Reference Morozova2004), Western Australia (Crockford Reference Crockford1957), Timor (Bassler Reference Bassler1929), and southern Thailand (Sakagami Reference Sakagami1968, Reference Sakagami1970, Reference Sakagami1973, Reference Sakagami1975, Reference Sakagami1999). Permian Northern Hemisphere basins and locations included Novaya Zemlya and the Russian Arctic (Morozova and Krutchinina Reference Morozova and Krutchinina1986), data in Morozova (Reference Morozova1970), Spitsbergen and Arctic Canada (Nakrem Reference Nakrem1994; Key et al. Reference Key, Thrane and Collins2001; Ernst and Nakrem Reference Ernst and Nakrem2007; Nakrem et al. Reference Nakrem, Błażejowski and Gaździcki2009), Primorsky Krai and Khabarovsk Krai (Romanchuk Reference Romanchuk1967; Romanchuk and Kiseleva Reference Romanchuk and Kiseleva1968; Kiseleva Reference Kiseleva1982), and Nevada, U.S.A. (Gilmour Reference Gilmour1962, Reference Gilmour2014; Gilmour and Snyder Reference Gilmour and Snyder1986, Reference Gilmour and Snyder2000; Gilmour et al. Reference Gilmour, McColloch and Wardlaw1997).

Paleolatitude for all species occurrence locations was determined to the nearest 5 Myr age interval. For stable craton locations, the online interactive tool of van Hindsbergen et al. (Reference van Hinsbergen, De Groot, van Schaik, Spakman, Bijl, Sluijs, Langereis and Brinkhuis2015) was used. For early and mid-Paleozoic Iapetus and Rheic Ocean terranes and blocks, the paleogeographic maps of Scotese (Reference Scotese2001), Golonka et al. (Reference Golonka, Bocharova, Ford, Edrich, Bednarczyk and Wildharber2003), and Golonka and Gawęda (Reference Golonka, Gawęda and Sharkov2012) were assessed, and a latitude was determined from van Hindsbergen et al. (Reference van Hinsbergen, De Groot, van Schaik, Spakman, Bijl, Sluijs, Langereis and Brinkhuis2015) for the nearest relevant stable craton. For exotic Tethyan and Panthalassa terranes of the late Paleozoic, paleolatitudes were estimated from Jadoul et al. (Reference Jadoul, Garzanti and Fois1990), Scotese (Reference Scotese2001), Shi (Reference Shi2006), Adams et al. (Reference Adams, Campbell and Griffin2007), Brayard et al. (Reference Brayard, Escarguel, Bucher and Brühwiler2009), and Metcalfe (Reference Metcalfe2013).

Statistical Analyses

Data were managed, BSI values calculated, graphs plotted, and summary statistics (mean, r2) derived in Excel. Normal distribution tests (Anderson-Darling) and correlation coefficients were performed in PAST v. 4.03 (Hammer et al. Reference Hammer, Harper and Ryan2001). A Pearson's correlation test was performed for data with a normal distribution; the nonparametric Spearman's rs was applied for data with a nonnormal distribution.

Results

In total, BSI and paleolatitude data were gathered on type species of 184 genera of Trepostomata (125 exhibiting ramose colony form) and 63 genera of Cryptostomata (all ramose) from the Ordovician to Triassic (Supplementary Table 1). Data for an additional 119 trepostome (all colony forms) species from the Permian were also gathered (Supplementary Table 2).

Trepostomata

The BSI values for the 184 foliose, ramose, massive, and encrusting trepostome type species range from 3.0 to 210.7 over the Tremadocian (Lower Ordovician) to Norian (Upper Triassic). Paleolatitudes for trepostome type species range from 50°N to 74.5°S. When plotted against normalized paleolatitude, BSI values show no clear trend, either as a group or when considered by morphological form (Fig. 2A). The most common zoarial habit of the Trepostomata is ramose (N = 125), and the BSI in this group also shows no statistically significant response to paleolatitude (rs = −0.104, p > 0.05) (Fig. 2B).

Figure 2. Bryozoan Skeletal Index (BSI) plotted against normalized paleolatitude. A, Trepostome genera (Ordovician to Triassic) differentiated by colony form. B, Ramose trepostome genera (Ordovician to Triassic) and cryptostome ramose genera (Ordovician to Permian).

For Ordovician to Devonian ramose taxa, there is a visible trend of highest BSI values at lower latitudes (Fig. 3A,C), however, this trend is not statistically significant, as low BSI values also occur at all latitudes. When BSI values are compared for each geologic period (Fig. 4A), weak trends of larger BSI at lower latitudes are apparent for the Ordovician and Devonian, with a slightly stronger relationship (rs = −0.670, p = < 0.05) for the Silurian, although over fewer genera. In contrast, the BSI values for Carboniferous to Triassic taxa are highest at higher latitudes (Fig. 3A,C), but again this is not statistically significant, as low BSI values also occur at all latitudes. When each period is assessed separately (Fig. 4B), all show weak positive correlation for higher BSI values at higher latitudes, with Permian taxa showing the strongest correlation (rs = 0.200) with marginal statistical significance (p > 0.05) (Fig. 4B). Permian trepostomes are considered in more detail in “Permian Trepostome BSI Parameters.”

Figure 3. Bryozoan Skeletal Index (BSI) for trepostome and cryptostome genera plotted against true paleolatitude. A, Trepostome bryozoans differentiated into Ordovician to Devonian and Carboniferous to Triassic. B, Cryptostome bryozoans differentiated into Ordovician to Devonian and Carboniferous to Permian. C, Violin and box plots showing paleolatitude distribution of Ordovician to Devonian and Carboniferous to Triassic cryptostomes and trepostomes at lower (<50) and higher (>50) BSI values. See color keys in A and B. Boxes show 25th to 75th percentiles, and horizontal bar shows the median.

Figure 4. Trepostome genera Bryozoan Skeletal Index (BSI) vs. normalized paleolatitude. A, Ordovician to Devonian, differentiated by period. B, Carboniferous to Triassic, differentiated by period.

Cryptostomata

BSI values range from 0.5 to 179.4 for the 82 ramose cryptostome genera from the Sandbian (Upper Ordovician) to Wordian (Guadalupian, Permian). The paleolatitudes of type species in 64 locations range between 48°N and 60.5°S. When plotted against normalized paleolatitude, BSI values show a weak but insignificant positive correlation (Fig. 2B). When BSI values are plotted by hemisphere, a distinct peak of higher values at lower latitudes is apparent (Fig. 3B). This distribution is broadly similar in both the Ordovician to Devonian and Carboniferous to Permian, where BSI values <50 are found over a range of paleolatitudes and those >50 are restricted to lower latitudes (Fig. 3C).

Permian Trepostome Species BSI

In total 98 ramose, 15 encrusting, 5 massive, and 1 foliose-only form were recorded. Plotted against normalized paleolatitude (Fig. 5A) massive forms show a clear positive correlation (rs = 0.872) of increasing BSI at higher latitudes; however, there are few data in this group. The correlations for encrusting and ramose forms are weakly positive (rs = 0.231 and 0.283, respectively) and significant (p < 0.001 and < 0.05, respectively). When BSI values are considered by hemisphere (Fig. 5B), the highest values are found in higher southern latitudes (i.e., southern Gondwana), with BSI ranging up to 632 (Stenopora rugosa Crockford, Reference Crockford1945) (mean = 90.9, SD = 112.1, n = 65). Northern Hemisphere BSI values range up to 195 (Tabulipora arcturusensis Gilmour, Reference Gilmour1962) (mean = 42.8, SD = 38.8, n = 54). A Spearman's correlation test for BSI in Southern Hemisphere shows a weak but significant correlation of increasing BSI with higher southern latitudes (rs = 0.313, p = 0.01) (Fig. 5B). The same test for Northern Hemisphere samples shows no correlation (p > 0.1).

Figure 5. Bryozoan Skeletal Index (BSI) for Permian trepostome species. A, Normalized paleolatitude differentiated by colony form. B, Northern and Southern Hemisphere BSI distribution, differentiated by colony form.

Permian Trepostome BSI Parameters

To investigate these high-latitude high BSI values, we assessed which parameters (EW, ZWT, and MZD) used in the BSI equation had the greatest influence on results. For Permian trepostome species, only the BSI parameter ZWT shows a normal distribution (Anderson-Darling p = > 0.1), and Pearson's correlation can be applied. Parameters EW and MZD have a nonnormal distribution (Anderson-Darling p = < 0.001 for both), and the nonparametric Spearman's correlation must be used. When the control these parameters have on BSI results is considered, exozone width has the strongest control (rs = 0.861, p = << 0.001), with thicker exozones resulting in higher BSI values (Fig. 6A). This is also partly reflected by higher BSI values with greater colony thickness (endozone + exozone). Calcite contributed from zooecial walls (ZWT) does not correlate to higher BSI values (R 2 = 0.011; Fig. 6B). Autozooecial aperture diameter (MZD), which accounts for space in the BSI calculation, does show a weak positive correlation (rs = 0.291, p < 0.05) whereby larger autozooecial apertures are linked to higher BSI values (Fig. 6C). Aperture diameter also increases with increasing southern paleolatitudes (rs = −0.472), but there is no apparent correlation in the Northern Hemisphere (rs = 0.032) (Fig. 6D).

Figure 6. Comparison of Bryozoan Skeletal Index (BSI) values to skeletal characters for Permian trepostome species of all colony forms. A, Exozone width (EW) vs. BSI. B, Zooecial wall thickness (ZWT) vs. BSI. C, Mean apertural diameter (MZD) vs. BSI. D, Mean apertural diameter (MZD) vs. normalized paleolatitude, plotted by BSI.

Discussion

The BSI approximates the relative amount of calcium carbonate precipitated within bryozoan colonies. In stable alkaline conditions, carbonate saturation in seawater and ease of precipitation of calcium carbonate decrease with temperature (and pressure) and thus are relatively lower at higher latitudes (Table 1). If carbonate saturation state influenced the amount of calcite precipitated per colony, it might be expected that there would be higher BSI values at lower paleolatitudes.

Table 1. Summary of anticipated response of bryozoans to carbonate saturation and observed response according to group and temporal range. BSI, Bryozoan Skeletal Index; Carb-Perm, Carboniferous to Permian; Carb-Trias, Carboniferous to Triassic; Ord-Dev, Ordovician to Devonian; Ord-Perm, Ordovician to Permian; Ord-Trias, Ordovician to Triassic.

Paleozoic Trepostome and Cryptostome Genera

Trepostome bryozoans when considered over the duration of the Ordovician to Triassic, show no apparent relationship between BSI and paleolatitude (Fig. 2). In other words, the BSI of trepostome taxa does not appear to be uniformly controlled by carbonate saturation state through the Paleozoic, just as trepostome taxa do not respond to calcite-aragonite sea transitions (Key et al. Reference Key, Wyse Jackson and Reid2022). When examined in more detail, however, earlier Paleozoic forms of the Ordovician to Devonian show, like the cryptostomes, a weak trend of higher BSI at lower latitudes (Figs. 3A,C, 4A). From the Carboniferous to the Triassic there is a trend of higher BSI values or more calcite per zooid at higher latitudes (Fig. 3C). This trend is weak for the Carboniferous and Triassic, but more pronounced for the Permian (Fig. 4B). In contrast, for cryptostome bryozoans, there is a clear peak of higher BSI values at lower latitudes (Fig. 3B,C), with lower BSI values at mid- and high latitudes. This pattern exists for both earlier Paleozoic (Ordovician to Devonian) and later Paleozoic (Carboniferous to Permian) forms regardless of hemisphere. Based on this observation, cryptostomes appear to have been more responsive to carbonate saturation state and to have precipitated more robustly calcified zoaria in warmer lower-latitude waters.

In the early Paleozoic, many continental blocks and their sedimentary basins were positioned equatorially (Scotese Reference Scotese2001). It is possible the trend of higher BSI values at lower latitudes may be an artifact of this paleogeography, with fossil records being concentrated equatorially. However, both cryptostome and trepostome taxa do range well into the midlatitudes (30°–60°) in the Ordovician and Devonian, and BSI values are lower (Figs. 3A,B, 4A). With the final amalgamation of Pangea by the late Paleozoic and its north–south orientation, continents and associated sedimentary basins extend into higher latitudes (Scotese Reference Scotese2001). While growth depth is not known for the species used here, they are likely mostly from the upper few hundred meters of bathymetry, and the gradient with respect to carbonate saturation would be weak. Additionally, if depositional depth was the control on BSI, species distribution with respect to paleolatitude should be random.

In the late Paleozoic the trepostomes with higher BSIs, range into higher latitudes; however, cryptostomes do not, and instead maintain a trend of higher BSI at lower latitudes (Table 1). Thus, it would appear that paleolatitude per se is not controlling BSI in bryozoans, but that bryozoans of these two ordinal groups respond to latitudinally driven oceanographic change differently. The Permian has a range of species present across high and low latitudes, especially in Gondwana, and this period is examined in more detail.

Permian Trepostome Species

Data on individual species were examined for the Permian, with the intention of sampling as wide a latitudinal range as possible. Trepostome species in the Permian Southern Hemisphere have distinctly higher BSI values at higher latitudes (Fig. 4B, Table 1). Modeled pCO2 and carbonate saturation state through the Phanerozoic reveal that, in this time interval, Permian carbonate saturation states were very similar to those of modern oceans (Riding and Liang Reference Riding and Liang2005; Berner Reference Berner2006; Mackenzie and Andersson Reference Mackenzie and Andersson2013). At these Permian latitudes (50°S–74°S), carbonate would have been relatively undersaturated with respect to aragonite and calcite, and sedimentologically, these higher southern latitudes record cold-water carbonates (Rogala et al. Reference Rogala, James and Reid2007; James and Lukasik Reference James, Lukasik, James and Dalrymple2010). Therefore, it should be metabolically more challenging to precipitate calcite skeletons at higher latitudes, and it would be expected that Permian trepostomes would be more lightly calcified and thus have lower BSI values.

While there are limited data on carbonate production and direct response to saturation state for modern bryozoans, Pentapora colonies are shown produce more carbonate per year in Mediterranean waters (Cocito and Ferdeghini Reference Cocito and Ferdeghini2001) than in cooler Atlantic waters (Lombardi et al. Reference Lombardi, Cocito, Hiscock, Occhipinti-Ambrogi, Setti and Taylor2008). Likewise, in the Southern Hemisphere, bryozoan colonies in cool temperate New Zealand waters (Smith et al. Reference Smith, Stewart, Key and Jamet2001) have been shown to produce more carbonate per year than Antarctic bryozoans (Smith Reference Smith2007). Furthermore, in summer growth bands of Pentapora, the weight percent of aragonite was higher than in winter growth periods (Lombardi et al. Reference Lombardi, Cocito, Hiscock, Occhipinti-Ambrogi, Setti and Taylor2008), suggesting bryozoans are also responsive to seasonal variation in saturation state of carbonate mineral species. Therefore, the premise that Permian forms should show less skeletal calcite (or lower BSI) at high latitudes is not without basis. So why is BSI higher at high latitudes rather than higher at low latitudes as might be expected?

When investigating the drivers of BSI values in the Permian data, the thickness of the exozone is the strongest predictor of BSI values (Fig. 6A). This is hardly surprising, as the thicker the exozone, the more calcite will be present. Interestingly, although the thickness of the wall arithmetically contributes positively to BSI, there is no correlative relationship (Fig. 6B). Examination of autozooecial aperture diameter (MZD), the parameter that accounts for space in the skeleton, reveals a positive relationship to BSI (Fig. 6C). It might be expected that larger apertures, representing more space in the skeleton, would reduce BSI.

The size of the aperture in modern cheilostome and cyclostome bryozoans is known to be correlated to the size of the mouth and lophophore of the soft-bodied zooid (Winston Reference Winston, Woollacott and Zimmer1977; Tamberg and Smith Reference Tamberg and Smith2020; Reid and Tamberg Reference Reid and Tamberg2021). In turn, the size of the mouth controls the size of food particles that can be ingested (Winston Reference Winston, Woollacott and Zimmer1977; McKinney and Jackson Reference McKinney and Jackson1991; Sanderson et al. Reference Sanderson, Thorpe, Clarke, Cubilla and Jackson2000). Larger lophophores are linked to higher pumping rates (Riisgård and Manriquez Reference Riisgård and Manríquez1997), which together would increase the food intake of larger-aperture bryozoans. We speculate that this increased feeding capacity is providing more caloric resources for precipitating more skeletal carbonate. While these polar Permian waters did not show evidence of seasonality in the skeletons (C.M.R. personal observation) common to modern temperate bryozoans, it cannot be discounted that the large aperture had an impact similar to what is reported in modern species, where aperture size increases with spring and autumn nutrient availability, driving zooid growth during these seasons (O'Dea Reference O'Dea2005; Key et al. Reference Key, Rossi, Smith, Hageman and Patterson2018).

As BSI increases with higher southern latitudes so does aperture size (Fig. 6D). This suggests that the correspondingly larger mouth and lophophore size and associated feeding abilities supported these high-latitude bryozoans to metabolically overcome the challenges of living in seawater undersaturated with respect to calcite and not only continue to precipitate but precipitate skeletons with more calcite. The same trend is not seen in Northern Hemisphere taxa, for which there are only data into the midlatitudes and few taxa have BSI values over 100 (Fig. 5B).

Permian high southern latitude species diversity of bryozoan faunas decreases with increasing latitude, as cystoporates and cryptostomes largely disappear, and the faunas are overwhelmingly composed of trepostomes and fenestrates (Reid and James Reference Reid, James, Hageman, Key and Winston2008). In comparison, low-latitude faunas include all orders, as do Northern Hemisphere low and midlatitude faunas of the Sverdrup and Arctic Basins (Reid and James Reference Reid and James2010). Thus, the near absence of cystoporates and cryptostomes from southern high-latitude Permian faunas allowed the trepostomes to diversify into this ecospace and take advantage of food resources not previously available to them (Reid and Tamberg Reference Reid and Tamberg2021). It appears that this access to additional resources and enhanced feeding rates in high latitudes also allowed trepostomes to metabolically mediate the additional challenges of reduced carbonate saturation at these latitudes. But to achieve this they must have been capable of biological mediation of skeletal precipitation in adverse saturation conditions. In modern bryozoans, feeding current speeds (Sanderson and Thorpe Reference Sanderson, Thorpe, Gordon, Smith and Grant-Mackie1996) and clearance rates of particles (Menon Reference Menon1974; Riisgård and Manriquez Reference Riisgård and Manríquez1997) increase with temperature, and therefore the larger mouths (apertures) in Permian high-latitude forms may have been a function of the need to increase the range of ingestible food particles to overcome slower rates (cf. Reid and Tamberg Reference Reid and Tamberg2021) and maintain stable calorific intake. There may be other causes for larger mouth size, such as overall larger polypide size or differing food resources, or the absence of competing cystoporates, as suggested by Reid and Tamberg (Reference Reid and Tamberg2021). It also needs to be asked what benefit trepostome bryozoans gained in precipitating more calcium carbonate given the lower calcite saturation states. Just because they may have had the caloric intake to do so, does not mean they did. It is worth noting that these southern high latitudes are known for large bryozoan colonies alongside a diverse brachiopod and molluscan fauna (Reid and James Reference Reid, James, Hageman, Key and Winston2008) and that the typical algal, sponge, and tabulate coral reef formers of the Permian (Kiessling Reference Kiessling2002) are absent at these high latitudes. Unitary brachiopods and mollusks are unable to grow far above the substratum, and in the absence of phototrophic reef-formers, the bryozoans may have been filling this ecospace.

If trepostome bryozoans, as discussed earlier, are capable of biological mediation of calcite precipitation through increased feeding to overcome lowered saturation states, the converse may also be true for the cryptostomes. Perhaps cryptostomes were unable to metabolically mediate calcite precipitation to overcome lower saturation states and were only successful at lower latitudes. The skeletal structure of fenestrate bryozoans does not align well with the BSI calculation and thus cannot be assessed in this way. The vesicular structure of cystoporate bryozoans, which is not usually numerically accounted for in systematic descriptions, also makes them difficult candidates for accurate BSI analysis. However, based on distribution patterns in the Permian Southern Hemisphere, it could be implied that fenestrates, like trepostomes, were also able to biologically mediate calcite precipitation in lower saturation states and that the cystoporates, like the cryptostomes, could not. Whereas it is possible that the ability of trepostomes to biologically overcome lower saturation states at higher latitudes through the Permian contributed to their survival of the end-Permian extinction and associated very low calcite saturation states (Jurikova et al. Reference Jurikova, Gutjahr, Wallmann, Flögel, Liebetrau, Posenato, Angiolini, Garbelli, Brand, Wiedenbeck and Eisenhauer2020), this would need to be examined in more detail across all Paleozoic bryozoan groups.

Implications for Modern Bryozoans

Paleozoic stenolaemate bryozoans appear to have had variable responses and capacity to respond to changing ocean chemistry. If the trepostome bryozoans respond differently than cryptostomes, we should not presume that modern stenolaemate (Cyclostomata) and gymnolaemate (Cheilostomata) behave in a uniform way with respect to ocean chemistry. In consideration of current ocean acidification concerns and the importance of bryozoans as habitat formers (Wood and Probert Reference Wood and Probert2013), each group needs to be investigated separately, and one should not expect all bryozoan groups to respond in the same way.

Conclusions

Paleozoic marine bryozoans had variable responses to paleolatitude and inferred carbonate saturation states. Cryptostome bryozoan genera precipitated the most calcite per colony at lower latitudes, where carbonate saturation states would be higher, and less in midlatitudes, where carbonate would be undersaturated. This implies they were unable to metabolically overcome the increased pressures of precipitating calcium carbonate at higher latitudes.

Trepostome bryozoan genera show a similar but weaker trend for the Ordovician to Devonian. However, in the Carboniferous to Triassic, they show a trend toward more calcium carbonate per colony at higher latitudes, indicating they were able to overcome unfavorable carbonate saturation states. Analysis of Permian trepostome species indicates this was most pronounced in the Southern Hemisphere, where they were able to metabolically overcome unfavorable carbonate saturation states at higher latitudes supported by increased feeding capacity.

The fact that trepostome and cryptostome bryozoans responded differently to carbonate saturation states shows that bryozoans cannot be treated as a single group in extinction events influenced by ocean chemistry and has important implications for modern bryozoans. Modern stenolaemate and gymnolaemate bryozoans need to be considered separately in studies of their response to ocean acidification.

Acknowledgments

We are grateful to C. Buttler, who provided access to the genus descriptions and plates for the forthcoming Trepostome volume of the Treatise on Invertebrate Paleontology. We thank S. Pruss and an anonymous reviewer for constructive feedback on the original article.

Data Availability Statement

Data available from the Dryad Digital Repository: https://doi.org/10.5061/dryad.1zcrjdfvm.

References

Literature Cited

Adams, C., Campbell, H., and Griffin, W.. 2007. Provenance comparisons of Permian to Jurassic tectonostratigraphic terranes in New Zealand: perspectives from detrital zircon age patterns. Geological Magazine 144:701–729.CrossRefGoogle Scholar
Barnes, D. K. A. 1995. Seasonal and annual growth in erect species of Antarctic bryozoans. Journal of Experimental Marine Biology and Ecology 188:181–198.CrossRefGoogle Scholar
Bassler, R. S. 1929. The Permian Bryozoa of Timor. Palaeontologie von Timor, XVI Lieferung 28:36–89.Google Scholar
Berner, R. A. 2006. GEOCARBSULF: a combined model for Phanerozoic atmospheric O2 and CO2. Geochimica et Cosmochimica Acta 70:5653–5664.CrossRefGoogle Scholar
Brayard, A., Escarguel, G., Bucher, H., and Brühwiler, T.. 2009. Smithian and Spathian (Early Triassic) ammonoid assemblages from terranes: paleoceanographic and paleogeographic implications. Journal of Asian Earth Sciences 36:420–433.CrossRefGoogle Scholar
Brey, T., Gutt, J., Mackensen, A., and Starmans, A.. 1998. Growth and productivity of the high Antarctic bryozoan Melicerita obliqua. Marine Biology 132:327–333.CrossRefGoogle Scholar
Cocito, S., and Ferdeghini, F.. 2001. Carbonate standing stock and carbonate production of the bryozoan Pentapora fascialis in the north-western Mediterranean. Facies 45:25–30.CrossRefGoogle Scholar
Cohen, K. M., Finney, S. C., Gibbard, P. L., and Fan, J.-X.. 2013. Updated: The ICS International Chronostratigraphic Chart. Episodes 36:199–204.CrossRefGoogle Scholar
Crockford, J. M. 1941. Permian Bryozoa of eastern Australia. Part II. New species from the Upper Marine Series of New South Wales. Journal and Proceedings of the Royal Society of New South Wales 74:502–516.Google Scholar
Crockford, J. M. 1943. Permian Bryozoa of eastern Australia. Part III. Batostomellidae and Fenestrellinidae from Queensland, New South Wales, and Tasmania. Journal and Proceedings of the Royal Society of New South Wales 76:260–266.Google Scholar
Crockford, J. M. 1945. Stenoporids from the Permian of New South Wales and Tasmania. Proceedings of the Linnean Society of New South Wales 70:9–24.Google Scholar
Crockford, J. M. 1957. Permian Bryozoa from the Fitzroy Basin, Western Australia. Bureau of Mineral Resources, Geology and Geophysics, Bulletin 34.Google Scholar
Ernst, A., and Nakrem, H. A.. 2007. Lower Permian Bryozoa from Ellesmere Island (Canada). Paläontologische Zeitschrift 81:17–28.CrossRefGoogle Scholar
Gilmour, E. H. 1962. A new species of Tabulipora from the Permian of Nevada. Journal of Paleontology 36:1019–1020.Google Scholar
Gilmour, E. H. 2014. Bryozoa of the uppermost Gerster Limestone (late Wordian, Permian), Medicine Range, northeastern Nevada, USA. Rocky Mountain Geology 49:137–165.CrossRefGoogle Scholar
Gilmour, E. H., and Snyder, E. M.. 1986. Stellahexaformis and Morozoviella, two new genera of Bryozoa from the Gerster Formation, northeastern Nevada. Contributions to Geology 24:211–217.Google Scholar
Gilmour, E. H., and Snyder, E. M.. 2000. Bryozoa of the Mission Argillite (Permian), northeastern Washington. Journal of Paleontology 74:545–570.2.0.CO;2>CrossRefGoogle Scholar
Gilmour, E. H., McColloch, M. E., and Wardlaw, B. R.. 1997. Bryozoa of the Murdock Mountain Formation (Wordian, Permian), Leach Mountains, northeastern Nevada. Journal of Paleontology 71:214–236.CrossRefGoogle Scholar
Golonka, J., and Gawęda, A.. 2012. Plate tectonic evolution of the southern margin of Laurussia in the Paleozoic. Pp. 261–282 in Sharkov, E., ed. Tectonics—recent advances. IntechOpen, London.Google Scholar
Golonka, J., Bocharova, N. Y., Ford, D., Edrich, M. E., Bednarczyk, J., and Wildharber, J.. 2003. Paleogeographic reconstructions and basins development of the Arctic. Marine and Petroleum Geology 20:211–248.CrossRefGoogle Scholar
Hammer, O., Harper, D. A. T., and Ryan, P. D.. 2001. PAST: Paleontological statistics software package for education and data analysis. Palaeontologia Electronica 4:1–9.Google Scholar
Jadoul, F., Garzanti, E., and Fois, E.. 1990. Upper Triassic Lower Jurassic stratigraphy and paleogeographic evolution of the Zanskar Tethys Himalaya (Zangla unit). Rivista Italiana di Paleontologia e Stratigrafia 95:351–396.Google Scholar
James, N. P., and Jones, B.. 2015. Origin of carbonate sedimentary rocks. Wiley, Hoboken, N.J.Google Scholar
James, N. P., and Lukasik, J.. 2010. Cool-and cold-water neritic carbonates. Pp. 369–398 in James, N. P., and Dalrymple, R. W., eds. Facies models 4. GEOtext 6, Geological Association of Canada, St. John's, NL, Canada.Google Scholar
Jurikova, H., Gutjahr, M., Wallmann, K., Flögel, S., Liebetrau, V., Posenato, R., Angiolini, L., Garbelli, C., Brand, U., Wiedenbeck, M., and Eisenhauer, A.. 2020. Permian–Triassic mass extinction pulses driven by major marine carbon cycle perturbations. Nature Geoscience 13:745–750.CrossRefGoogle Scholar
Key, M. M. Jr., Thrane, L., and Collins, J. A.. 2001. Space-filling problems in ramose trepostome bryozoans as exemplified in a giant colony from the Permian of Greenland. Lethaia 34:125–135.CrossRefGoogle Scholar
Key, M. M. Jr., Wyse Jackson, P. N., Hakansson, E., Patterson, W. P., and Moore, M. D.. 2005. Gigantism in Permian trepostomes from Greenland: testing the algal symbiosis hypothesis using D13C and D18O values. Pp. 141–151 in Moyano, H. I. G., Cancino, J. M., and Wyse Jackson, P. N., eds. Bryozoan Studies 2004. Taylor and Francis, London.Google Scholar
Key, M. M. Jr., Rossi, R. K., Smith, A. M., Hageman, S. J., and Patterson, W. P.. 2018. Stable isotope profiles of skeletal carbonate validate annually-produced growth checks in the bryozoan Melicerita chathamensis from Snares Platform, New Zealand. Bulletin of Marine Science 94:1447–1464.Google Scholar
Key, M. M. Jr., Wyse Jackson, P. N., and Reid, C. M.. 2022. Trepostome bryozoans buck the trend and ignore calcite-aragonite seas. Palaeobiodiversity and Palaeoenvironments 102:253–263.CrossRefGoogle Scholar
Kiessling, W. 2002. Secular variations in the Phanerozoic reef ecosystem. In W. Kiessling, E. Flügel, and J. Golonka, eds. Phanerozoic reef patterns. SEPM Society for Sedimentary Geology 72:625–690.CrossRefGoogle Scholar
Kiseleva, A. V. 1982. New late Permian trepostomids from the Southern Primor'ye region. Paleontological Journal 16:74–81.Google Scholar
Lombardi, C., Cocito, S., Occhipinti-Ambrogi, A., and Hiscock, K.. 2006. The influence of seawater temperature on zooid size and growth rate in Pentapora fascialis (Bryozoa: Cheilostomata). Marine Biology 149:1103–1109.CrossRefGoogle Scholar
Lombardi, C., Cocito, S., Hiscock, K., Occhipinti-Ambrogi, A., Setti, M., and Taylor, P.. 2008. Influence of seawater temperature on growth bands, mineralogy and carbonate production in a bioconstructional bryozoan. Facies 54:333–342.CrossRefGoogle Scholar
Ma, J.-Y., Buttler, C. J., and Taylor, P. D.. 2014. Cladistic analysis of the ‘trepostome’ Suborder Esthonioporina and the systematics of Paleozoic bryozoans. Pp. 153–161 in Rosso, A., Wyse Jackson, P. N., and Porter, J., eds. Bryozoan studies 2013. Studi Trentini di Scienze Naturali, Trento.Google Scholar
Mackenzie, F. T., and Andersson, A. J.. 2013. Deep time; modelling of atmospheric CO2 and the marine CO2 -carbonic acid-carbonate system. Geochemical Perspectives 2:56–80.Google Scholar
McKinney, F. K., and Jackson, J. B.. 1991. Bryozoan evolution. University of Chicago Press, Chicago.Google Scholar
Menon, N. 1974. Clearance rates of food suspension and food passage rates as a function of temperature in two North-Sea bryozoans. Marine Biology 24:65–67.CrossRefGoogle Scholar
Metcalfe, I. 2013. Gondwana dispersion and Asian accretion: tectonic and palaeogeographic evolution of eastern Tethys. Journal of Asian Earth Sciences 66:1–33.CrossRefGoogle Scholar
Morozova, I. 1970. Late Permian Bryozoa. Transactions of the Paleontological Institute, Akademii Nauk, USSR 122:1–347.Google Scholar
Morozova, I. P. 2004. New Early Permian bryozoans of eastern Australia. Paleontological Journal 38:381–392.Google Scholar
Morozova, I. P., and Krutchinina, O. N.. 1986. Permskiye mshanki Arktiki (zapadnyy sektor) (Permian Bryozoa of the Arctic region; western sector). Izd. Nauka, Moscow. [In Russian.]Google Scholar
Nakrem, H. A. 1994. Middle Carboniferous–Lower Permian bryozoans from Spitsbergen. Acta Palaeontologica Polonica 39:45–116.Google Scholar
Nakrem, H. A., Błażejowski, B., and Gaździcki, A.. 2009. Lower Permian bryozoans from southern and central Spitsbergen, Svalbard. Acta Palaeontologica Polonica 54:677–698.CrossRefGoogle Scholar
O'Dea, A. 2005. Zooid size parallels contemporaneous oxygen isotopes in a large colony of Pentapora foliacea (Bryozoa). Marine Biology 146:1075–1081.CrossRefGoogle Scholar
Patzgold, J., Ristedt, H., and Wefer, G.. 1987. Rate of growth and longevity of a large colony of Pentapora foliacea (Bryozoa) recorded in their oxygen isotope profiles. Marine Biology 96:535–538.CrossRefGoogle Scholar
Reid, C. M. 2001. The Permian Bryozoa of Tasmania, New South Wales and southern Thailand: their taxonomy, biostratigraphy, palaeoecology and biogeography. Unpublished Ph.D. thesis. University of Tasmania, Australia. https://eprints.utas.edu.au/21360.Google Scholar
Reid, C. M. 2003. Permian Bryozoa of Tasmania and New South Wales: systematics and their use in Tasmanian biostratigraphy. Association of Australasian Palaeontologists Memoir 28:133.Google Scholar
Reid, C. M., and James, N. P.. 2008. Climatic response of Late Paleozoic bryozoans: diversity and composition of Gondwanan faunas. Pp. 243–250 in Hageman, S. J., Key, M. M. Jr., and Winston, J. E., eds. Bryozoan Studies 2007. Virginia Museum of Natural History Special Publication. Virginia Museum of Natural History, Martinsville.Google Scholar
Reid, C. M., and James, N. P.. 2010. Permian higher latitude bryozoan biogeography. Palaeogeography, Palaeoclimatology, Palaeoecology 298:31–41.CrossRefGoogle Scholar
Reid, C. M., and Tamberg, Y.. 2021. Trophic partitioning and feeding capacity in Permian bryozoan faunas of Gondwana. Palaeontology 64:555–572.CrossRefGoogle Scholar
Riding, R., and Liang, L.. 2005. Geobiology of microbial carbonates: metazoan and seawater saturation state influences on secular trends during the Phanerozoic. Palaeogeography, Palaeoclimatology, Palaeoecology 219:101–115.CrossRefGoogle Scholar
Riisgård, H. U., and Manríquez, P.. 1997. Filter-feeding in fifteen marine ectoprocts (Bryozoa): particle capture and water pumping. Marine Ecology Progress Series 154:223–239.CrossRefGoogle Scholar
Rogala, B., James, N. P., and Reid, C. M.. 2007. Deposition of polar carbonates during interglacial high-stands on an Early Permian shelf, Tasmania. Journal of Sedimentary Research. 77:587–607.CrossRefGoogle Scholar
Romanchuk, T. V. 1967. New bryozoans of the Order Trepostomata of the Upper Permian of the Khabarovsk Territory. Paleontological Journal 1967(2):59–63.Google Scholar
Romanchuk, T. V., and Kiseleva, A. V.. 1968. New late Permian bryozoans of the Far East. Paleontological Journal 4:488–492.Google Scholar
Sakagami, S. 1968. Permian Bryozoa from Khao Ta Mong Rai, peninsular Thailand. Geology and Palaeontology of Southeast Asia 5:47–67.Google Scholar
Sakagami, S. 1970. Addition to the Permian Bryozoa from Ko Muk, peninsular Thailand. Geology and Palaeontology of Southeast Asia 8:43–68.Google Scholar
Sakagami, S. 1973. Permian Bryozoa from Khao Raen, near Rat Buri, Thailand. Geology and Palaeontology of Southeast Asia 12:75–89.Google Scholar
Sakagami, S. 1975. Permian Bryozoa from Khao Hin Kling, near Phetchabun, north-central Thailand. Geology and Palaeontology of Southeast Asia 16:33–43.Google Scholar
Sakagami, S. 1999. Permian bryozoans from some localities in the Khao Hin Kling Area near Phetchabun, north-central Thailand. Bulletin of the Kitakyushi Museum of Natural History 18:77–103.Google Scholar
Sanderson, W. G., and Thorpe, J. P.. 1996. Effects of temperature on the feeding activity of some temperate intertidal Bryozoa. Pp. 271–282 in Gordon, D. P., Smith, A. M., and Grant-Mackie, J. A., eds. Bryozoans in space and time. NIWA, Wellington, New Zealand.Google Scholar
Sanderson, W. G., Thorpe, J. P., and Clarke, A.. 2000. Aspects of structure and function in the feeding of the Antarctic cheilostomate bryozoan Himantozoum antarcticum (Calvet). Pp. 355–364 in Cubilla, A. Herrera and Jackson, J. B. C., eds. Eleventh International Bryozoology Association Conference. Smithsonian Tropical Research Institute, Balboa.Google Scholar
Scotese, C. 2001. PALEOMAP website. http://scotese.com, accessed August 2021.Google Scholar
Shi, G. R. 2006. The marine Permian of East and Northeast Asia: an overview of biostratigraphy, palaeobiogeography and palaeogeographical implications. Journal of Asian Earth Sciences 26:175–206.CrossRefGoogle Scholar
Smith, A. M. 2007. Age, growth and carbonate production by erect rigid bryozoans in Antarctica. Palaeogeography, Palaeoclimatology, Palaeoecology 256:86–98.CrossRefGoogle Scholar
Smith, A. M., Stewart, B., Key, M. M. Jr., and Jamet, C. M.. 2001. Growth and carbonate production by Adeonellopsis (Bryozoa, Cheilostomata) in Doubtful Sound, New Zealand. Palaeogeography, Palaeoclimatology, Palaeoecology 175:201–210.CrossRefGoogle Scholar
Stanley, S. M., and Hardie, L. A.. 1998. Secular oscillations in the carbonate mineralogy of reef-building and sediment-producing organisms driven by tectonically forced shifts in seawater chemistry. Palaeogeography, Palaeoclimatology, Palaeoecology 144:3–19.CrossRefGoogle Scholar
Stanley, S. M., and Hardie, L. A.. 1999. Hypercalcification: paleontology links plate tectonics and geochemistry to sedimentology. GSA Today 9:1–7.Google Scholar
Tamberg, Y., and Smith, A. M.. 2020. In search of predictive models for stenolaemate morphometry across the skeletal–polypide divide. Paleobiology 46:218–236.CrossRefGoogle Scholar
Taylor, P. D. 1994. An early cheilostome bryozoan from the Upper Jurassic of Yemen. Neues Jahrbuch für Geologie und Paläontologie. Abhandlungen 191:331–344.Google Scholar
Taylor, P. D. 2020. Bryozoan paleobiology. Wiley, Hoboken, N.J.CrossRefGoogle Scholar
Taylor, P. D., and Allison, P. A.. 1998. Bryozoan carbonates through time and space. Geology 26:459–462.2.3.CO;2>CrossRefGoogle Scholar
Taylor, P. D., and Kuklinski, P.. 2011. Seawater chemistry and biomineralization: did trepostome bryozoans become hypercalcified in the “calcite sea” of the Ordovician? Palaeobiodiversity and Palaeoenvironments 91:185–195.CrossRefGoogle Scholar
Taylor, P. D., James, N. P., Bone, Y., Kuklinski, P., and Kyser, T. K.. 2009. Evolving mineralogy of cheilostome bryozoans. Palaios 24:440–452.CrossRefGoogle Scholar
van Hinsbergen, D. J., De Groot, L. V., van Schaik, S. J., Spakman, W., Bijl, P. K., Sluijs, A., Langereis, C. G., and Brinkhuis, H.. 2015. A paleolatitude calculator for paleoclimate studies. PLoS ONE 10(6):e0126946.CrossRefGoogle ScholarPubMed
Wass, R. E. 1968. Permian Polyzoa from the Bowen Basin. Bureau of Mineral Resources, Geology and Geophysics, Bulletin 90.Google Scholar
Winston, J. E. 1977. Feeding in marine bryozoans. Pp. 233–272 in Woollacott, R. M. and Zimmer, R. L., eds. Biology of bryozoans. Academic Press, New York.CrossRefGoogle Scholar
Wood, A., and Probert, P.. 2013. Bryozoan-dominated benthos of Otago shelf, New Zealand: its associated fauna, environmental setting and anthropogenic threats. Journal of the Royal Society of New Zealand 43:231–249.CrossRefGoogle Scholar
Wyse Jackson, P. N., Key, M. M. Jr., and Reid, C. M.. 2020. Bryozoan Skeletal Index (BSI): a measure of the degree of calcification in stenolaemate bryozoans. Pp. 193–206 in Wyse Jackson, P. N. and Zagorsek, K., eds. Bryozoan Studies 2019. Czech Geological Survey, Prague.Google Scholar
Zhang, Z., Zhang, Z., Ma, J., Taylor, P. D., Strotz, L. C., Jacquet, S. M., Skovsted, C. B., Chen, F., Han, J., and Brock, G. A.. 2021. Fossil evidence unveils an early Cambrian origin for Bryozoa. Nature 599:251–255.CrossRefGoogle ScholarPubMed
Figure 0

Figure 1. Morphological characters used to derive the Bryozoan Skeletal Index (BSI) on a ramose zoarium. From Wyse Jackson et al. (2020: fig. 2). Abbreviations: EW, exozone width; MZD, autozooecial aperture diameter; ZWT, zooecial wall thickness.

Figure 1

Figure 2. Bryozoan Skeletal Index (BSI) plotted against normalized paleolatitude. A, Trepostome genera (Ordovician to Triassic) differentiated by colony form. B, Ramose trepostome genera (Ordovician to Triassic) and cryptostome ramose genera (Ordovician to Permian).

Figure 2

Figure 3. Bryozoan Skeletal Index (BSI) for trepostome and cryptostome genera plotted against true paleolatitude. A, Trepostome bryozoans differentiated into Ordovician to Devonian and Carboniferous to Triassic. B, Cryptostome bryozoans differentiated into Ordovician to Devonian and Carboniferous to Permian. C, Violin and box plots showing paleolatitude distribution of Ordovician to Devonian and Carboniferous to Triassic cryptostomes and trepostomes at lower (<50) and higher (>50) BSI values. See color keys in A and B. Boxes show 25th to 75th percentiles, and horizontal bar shows the median.

Figure 3

Figure 4. Trepostome genera Bryozoan Skeletal Index (BSI) vs. normalized paleolatitude. A, Ordovician to Devonian, differentiated by period. B, Carboniferous to Triassic, differentiated by period.

Figure 4

Figure 5. Bryozoan Skeletal Index (BSI) for Permian trepostome species. A, Normalized paleolatitude differentiated by colony form. B, Northern and Southern Hemisphere BSI distribution, differentiated by colony form.

Figure 5

Figure 6. Comparison of Bryozoan Skeletal Index (BSI) values to skeletal characters for Permian trepostome species of all colony forms. A, Exozone width (EW) vs. BSI. B, Zooecial wall thickness (ZWT) vs. BSI. C, Mean apertural diameter (MZD) vs. BSI. D, Mean apertural diameter (MZD) vs. normalized paleolatitude, plotted by BSI.

Figure 6

Table 1. Summary of anticipated response of bryozoans to carbonate saturation and observed response according to group and temporal range. BSI, Bryozoan Skeletal Index; Carb-Perm, Carboniferous to Permian; Carb-Trias, Carboniferous to Triassic; Ord-Dev, Ordovician to Devonian; Ord-Perm, Ordovician to Permian; Ord-Trias, Ordovician to Triassic.