Temperature-related body size change of marine benthic macroinvertebrates across the Early Toarcian Anoxic Event

Abstract

The Toarcian Oceanic Anoxic Event (TOAE, Early Jurassic, ~182 Ma ago) was characterised by severe environmental perturbations which led to habitat degradation and extinction of marine species. Warming-induced anoxia is usually identified as main driver, but because marine life was also affected in oxygenated environments the role of raised temperature and its effects on marine life need to be addressed. Body size is a fundamental characteristic of organisms and is expected to decrease as a response to heat stress. We present quantitative size data of bivalves and brachiopods across the TOAE from oxygenated habitats in the Iberian Basin, integrated with geochemical proxy data (δ13C and δ18O), to investigate the relationship between changes in temperature and body size. We find a strong negative correlation between the mean shell size of bivalve communities and isotope-derived temperature estimates, suggesting heat stress as a main cause of body size reduction. While within-species size changes were minor, we identify changes in the abundance of differently sized species as the dominant mechanism of reduced community shell size during the TOAE. Brachiopods experienced a wholesale turnover across the early warming phase and were replaced by a virtually monotypic assemblage of a smaller-sized, opportunistic species.

Introduction

Growth, and hence body size of organisms, is affected by both biotic and abiotic factors. Body size decrease in particular is observed during and after episodes of warming in modern and extinct taxa (e.g. refs. 1,2,3,4). Temperature increase has complex and wide-ranging effects on organisms5,6. Once temperature surpasses the optimal thermal range of an organism it can result in decreased growth, reproduction and feeding rates up to the collapse of all biological functions7. Body size decrease has thus been suggested as a third universal response to warming8 in addition to changes in the geographic distribution of species and in phenological events1,9.

We focus on changes in shell size of marine benthic macroinvertebrates across the Early Toarcian Oceanic Anoxic Event (TOAE; Early Jurassic, ~182 Ma)10. Only a few studies have addressed this topic, mostly focusing on anoxic settings11,12,13,14,15. Marine oxygen depletion has usually been considered the prime causal mechanism of increased early Toarcian extinction rates and faunal turnover16,17,18. Nevertheless, elevated extinction intensities and body size decrease before and across the TOAE have been registered also in well-aerated shallow-shelf settings in the western Tethys (e.g. refs. 19,20,21,22). This implies that regional environmental differences existed during the TOAE23, and that anoxia alone cannot be considered a universal and single driver of the associated biotic crisis. High temperatures during the TOAE have been suggested as an important factor in oxic settings20,21,24. However, statistical tests of causal links between fluctuating temperatures with diversity and community composition are exceedingly rare (but see refs. 25,26) and so far are lacking regarding the relation between temperature and body size.

We quantitatively evaluate the role of temperature for changes in body size of bivalves and brachiopods from an oxygenated setting in the Iberian Range of Spain. Specifically, we test whether body size is reduced during the hyperthermal conditions of the TOAE, and to which degree body size is correlated negatively with ambient water temperatures. We focus on changes of the average shell size of bivalve-brachiopod communities through time. Essentially, heat stress-induced reductions in mean shell size at the community level can be caused by two mechanism: (1) a decrease in shell size within species as known from the physiological response of modern organisms, and/or (2) a change in species composition, with smaller-sized species replacing or becoming more abundant than larger-sized species.

We obtained body size trajectories by plotting the mean shell size of specimens per faunal sample for bivalve-brachiopod communities as a whole and separately for the bivalve and brachiopod subcommunities and for individual species. Changes in shell size were tested for correlation with the δ18O time series, our geochemical proxy for ambient water temperatures, derived from rhynchonellid brachiopods and oyster shells from the same levels as the faunal data. We performed Generalized Least Squares (GLS) fitting on a direct correlation of body size and δ18O (here termed lag 0) and on a lagged isotope time series (here termed lag 1), i.e. correlating each body size value with the δ18O value of the immediately preceding sample, to test for a delayed response of body size to temperature.

Studied Section and Environmental Conditions

We studied a ca. 28-m-thick sedimentary succession at Barranco de la Cañada (40°23′53.4″N 1°30′07.4″W) near Albarracín, Spain (Fig. 1), where the Toarcian Turmiel Formation27 is characterised by rhythmic alternations of marlstones and partly argillaceous limestones. The latter primarily comprise mudstones, wackestones, and floatstones indicative of low-energy conditions below storm wave base at an estimated water depth of 40–70 m28,29,30. Packstones and rudstones are very rare, suggesting transient episodes of higher water energy, interpreted as distal storm flow beds19. Deposition took place in a well-oxygenated mid-ramp setting. Black shales typical for the TOAE elsewhere are absent. The section has a well-defined biozonation based on ammonites and brachiopods31, and is highly fossiliferous, with abundant benthic macroinvertebrates (Fig. 2). The studied interval ranges from the Pliensbachian/Toarcian boundary to the lower Bifrons Zone of the middle Toarcian. We identified the TOAE chemostratigraphically using the characteristic negative carbon-isotope excursion (CIE)16 obtained from well-preserved shells of rhynchonellid brachiopods and oysters (Fig. 3). The TOAE thus spans the uppermost Tenuicostatum Zone up to the lower Serpentinum Zone.

Figure 1
figure1

Geographic location of the studied section at Barranco de la Cañada (a) and Early Jurassic palaeogeographic reconstruction of the NW Tethys (b). Location of the studied area is marked with a black star. Palaeomap modified from Fig. 1 in ref. 17 (software used: Adobe Illustrator v. CS6 [https://www.adobe.com/de/products/illustrator.html]).

Figure 2
figure2

Stratigraphic ranges of benthic macroinvertebrate species at Barranco de la Cañada. The taxa have been ordered by last occurrences, and subdivided into the main taxonomical groups. Each point represents the presence of a taxon in a sampled level. The star-shaped symbols indicate the sampled levels. The chemostratigraphically defined TOAE interval is represented by the shaded grey area. Chronostratigraphic boundaries modified from ref. 28.

Figure 3
figure3

Stratigraphy, mean shell size of all individuals of the three main analysed faunal groupings by sample, and geochemical data (δ18O and δ13C) of the Barranco de la Cañada succession. The TOAE (grey shading) represents the extent of the globally recognised negative δ13C isotopic excursion. Horizontal bars in the shell size time series represent the interquartile range delimited by the first and third quartiles, while in the isotope time series they represent the double standard error for each sample. A three-point moving average (solid black line) was fitted to the faunal data alongside the point-by-point trend (dashed grey line). Isotope data after ref. 32 and temperature change ΔT, relative to the lowermost value recorded in the profile, is estimated from the equation in ref. 35. Third-order transgressive-regressive cycles from refs. 29,30. Abbreviations: Falcif. = Falciferum; Mid. To. = Middle Toarcian; Pa. = Paltum; Semicelat. = Semicelatum; Sublevi. = Sublevisoni; Tenuicostat. = Tenuicostatum.

Oxygen isotope ratios from the same specimens provide a record of palaeotemperatures at the seafloor. Across the studied interval the measured isotope ratios indicate a rapid increase in temperatures when the negative CIE of the TOAE commenced. Palaeotemperatures then stayed stable and high until the end of the negative CIE, where a brief return to pre-excursion temperatures is indicated. The upper part of the section is then characterised by a slight warming, resulting in average water temperatures intermediate between earliest Toarcian temperatures and those during the negative CIE. Temperature estimates indicate that palaeotemperatures were elevated by ~3.5 °C throughout the TOAE32 (Fig. 3; see Methods and Fig. S1 for details).

In terms of sequence stratigraphy (summarized in refs. 28,29,30,33) the studied interval is part of a second-order transgressive-regressive cycle (LJ-3 in ref. 30) ranging from the early Pliensbachian (Davoei Zone) to the middle Toarcian (Variabilis Zone). The transgressive phase occurred in three distinct pulses, of which the second (LJ3-2) and parts of the third (LJ3-3) third order transgressive-regressive cycle fall within the study interval30 (Fig. 3).

Results

Changes in shell size

A temporary decrease in mean shell size during the TOAE is clearly evident in the high-resolution trajectories of the bivalve-brachiopod communities and subcommunities (Fig. 3). They illustrate that the brachiopod and bivalve subcommunities start becoming smaller-sized at different times. Shell size of bivalve subcommunities starts to decrease at the beginning of the TOAE simultaneously with the first shift to warmer temperatures, whereas brachiopod subcommunities only get smaller in the later part of the TOAE. The re-establishment of pre-TOAE shell sizes of all community types occurred synchronously and rapidly at the termination of the TOAE (Fig. 3). This rapid recovery of mean body size corresponds to a distinct shift to cooler temperatures, suggesting an important role of warming in controlling reductions in shell size and of cooling in the subsequent return to original size distributions.

Within-species size patterns of the more common species, i.e. those 34 species that occur with at least three specimens per level and at least at three sampling levels, are different for bivalves and brachiopods (Fig. 4). Most of the common brachiopod species are confined to either the pre-TOAE, the TOAE, or the post-TOAE interval (Figs. 2 and 4). Only three common species extend from pre-TOAE times into the lower part of the TOAE before they disappear without appreciable change in shell size (Fig. 4). In the upper part of the TOAE they are replaced by the relatively small-sized brachiopod Soaresirhynchia bouchardi. Bivalve species, by contrast, commonly occur in two or all three intervals (Figs. 2 and 4). Unequivocal indication for consistently reduced size of individual bivalve species during the TOAE hyperthermal is missing. Yet, several species show a moderate size decrease at the beginning of the TOAE relative to the preceding sampling levels (Gryphaea (B.) sublobata, Nicaniella voltzi, Pinna cf. folium, Plagiostoma giganteum, Pronoella intermedia, Pseudolimea duplicata, Pseudopecten dentatus) or a size increase from the end of the TOAE into the early post-TOAE phase (Entolium corneolum, Grammatodon concinnus, Parallelodon hirsonensis, Pseudolimea duplicata).

Figure 4
figure4

Mean shell size of all individuals by sample of bivalve and brachiopod species present in at least three levels and with at least three specimens per sample. Interquartile ranges represented by the black horizontal lines. TOAE represented by the grey shading. n = total number of individuals.

Abundance change of larger-sized versus smaller-sized species

To assess the impact of changes in the relative abundance of differently sized species for size change at the community scale, we grouped the common species into “smaller-sized” and “larger-sized” using the mean of all species’ mean shell sizes as the cut-off value (see Methods, Supplementary Fig. S2). Of the 34 common species, 19 are categorized as larger-sized (11 bivalves, 8 brachiopods) and 15 as smaller-sized (10 bivalves, 5 brachiopods). To facilitate comparison we plotted the percentage of individuals of larger-sized species per sample next to the already established trajectories of mean community shell size and of inferred bottom water temperature change (Fig. 5 and Supplementary Fig. S3). For bivalve-brachiopod communities, overall trends in mean shell size and in abundance of larger-sized species are strikingly similar and significantly correlated (Table 1). Clearly, the transient decrease in mean community level shell size during the TOAE is associated with a decline in the relative abundance of larger-sized species. Similar patterns are evident in bivalve and brachiopod subcommunities (Table 1), where a decline in the abundance of larger-sized species during the TOAE is reflected by smaller community shell sizes than during pre-TOAE times (Fig. 5 and Supplementary Fig. S3).

Figure 5
figure5

Relative abundance, expressed in percentage, of all individuals of larger-sized species in each sample for the whole bivalve–brachiopod community and for bivalves. The two time series are plotted alongside the mean shell size of the corresponding group and the δ18O isotope time series from Fig. 3. For further explanations, see Fig. 3.

Table 1 Results of the Generalized Least Squares (GLS) correlation between shell size and relative abundance of individuals of larger-sized species for the three analyzed groups (brachiopod + bivalve community; brachiopod and bivalve subcommunities).

Correlation of shell size and species abundance with temperature

Tests for autocorrelation and stationarity of the faunal and isotope data (see Methods and Supplementary Tables S1S4) did not flag any caveats for the applicability of GLS regression on the original body size time series, while differencing was necessary when the relative abundance of larger-sized species was part of the model. The correlation of δ18O values and shell size of bivalve-brachiopod communities is significant at lag 1, suggesting that the temperature at one sample level was influencing shell size in the next younger sample (Table 2). Correlation at lag 0, by contrast, is not significant. For the bivalve subcommunities, body size is significantly correlated with δ18O for both lag 0 and lag 1, while in brachiopods the correlation is non-significant in both cases (Table 2). These results, along with differences in the timing of size changes, hint at a decoupled response to changes in water temperature of these two groups. Regarding the relative abundances of larger-sized species, results for bivalve-brachiopod communities and bivalve subcommunities show significant correlations with δ18O at lag 0 (Table 2).

Table 2 Results of the Generalized Least Squares (GLS) correlation between shell size/ percentage of larger-sized individuals and δ18O for the analyzed faunal groups.

Discussion

Excluding biases in size frequency distributions

Habitat change can be a potential source of bias when investigating body size trends, as variations in body size can originate from facies changes due to fluctuations in relative sea level. If body size were primarily controlled by changes in sea level, we would expect similar fluctuations in size in each transgressive-regressive cycle. Because this is not the case (Fig. 3), and the represented depositional environments stayed below or close to storm wave base throughout the studied time interval, we conclude that fluctuations in sea level and depositional environments did not generally drive the observed variations in shell size. Furthermore, lack of size sorting and the absence of preferential orientations of shells suggest that post-mortal shell transport was minor and that the frequency distributions of shell size were not modified by currents or waves. We infer that the observed size patterns were not driven by changes in relative sea level and depositional environments, and were not biased by taphonomic processes, but rather demonstrate a negative effect of rising temperatures on shell size of benthic macroinvertebrate assemblages.

Alternative factors causing the size changes

Apart from heat stress, the observed reductions in community-level shell size could also be caused by other stressors – in particular reduced oxygen concentrations, ocean acidification, low food supply, and seawater freshening – and these factors could have acted in synergy.

Salinity

Potential changes in salinity are relevant not only because they could provoke size decrease34 but because they would affect the oxygen isotope composition of seawater and thereby affect our temperature estimates. Palaeotemperatures from δ18O values in fossil calcite are calculated using equations that require an estimate of the isotopic composition of ambient seawater. Whilst the oxygen isotope thermometer of ref. 35 is linear and therefore insensitive to the exact δ18O value of the local seawater, biased temperature information may nevertheless derive from substantial salinity changes across the studied time interval.

The magnitude of the oxygen isotope shift from the earliest Toarcian to the TOAE is 1.00 ± 0.09‰ for the studied site. To explain such a shift purely by salinity change, strong freshening of the local water mass would have had to occur. Comparison of the Spanish isotope record to multiple correlative records from other European basins suggests that large scale freshening of waters for which there is some evidence in central and northern Europe (e.g., ref. 36) is much more subdued in Spain, if at all present37,38. In a shallow, but open marine shelf setting facing deep marine Tethyan basins to the South East (e.g., ref. 39), sustained salinity reduction is much less likely to have occurred than in the more restricted subbasins of the Laurasian seaway further north.

At palaeolatitudes of ~25 °N, as reconstructed for the studied basin (Fig. 1; ref. 39), annual average meteoric water signatures are very unlikely to have been < −5‰40. Salinity-induced reduction of ambient water δ18O values is therefore expected to be 0.1‰ per psu or less. Lethally low salinity levels for the consistently observed stenohaline fauna (ammonites, crinoids, and rhynchonelliform brachiopods are continuously present throughout the section and specifically in the TOAE interval) would have occurred already much before ambient water δ18O would have changed by 1‰. We therefore conclude that large salinity changes are not compatible with faunal assemblages, considerations of meteoric signals, and comparison to other European basins. Consequently, we interpret the vast majority of the measured oxygen isotope signals during the TOAE to be a consequence of temperature change.

Hypoxia

Regarding the oxygen concentrations of bottom waters there is no evidence of severe hypoxia in the benthic environments of Barranco de la Cañada. Black shales, commonly characterising the TOAE elsewhere, are absent, shelly macroinvertebrates are ubiquitous, and bioturbation is common with a diverse suite of ichnotaxa (Spongeliomorpha, Thalassinoides, Palaeophycus, Rhizocorallium, Sphaerichnus, Trichichnus) in the TOAE interval (ref. 28; own observations). The ichnogenera Spongeliomorpha and Thalassinoides are produced by crustaceans, and because this faunal group is sensitive to hypoxia41, their appearance is independent evidence against low-oxygen conditions on and within the seafloor22.

Other environmental factors

As a direct consequence of elevated levels of CO2 in the atmosphere, global warming is commonly associated with ocean acidification. From experiments with modern species it appears that bivalves are more negatively affected by ocean acidification than articulate brachiopods22,42,43. This pattern of inferred physiological pH tolerance of bivalves and brachiopods does not conform with the Early Toarcian faunal pattern at Barranco de la Cañada, where most brachiopod species went extinct during the TOAE24 (see Discussion below). Thus, acidification cannot be inferred from the faunal patterns at Barranco de la Cañada, but independent signs of ocean acidification, such as changes in the boron isotope composition, should be investigated. Finally, a decline in primary productivity could be a stressor affecting specifically species with high energy demands such as active and/or large-sized taxa. The selective extinction of brachiopods argues against a low-productivity scenario because their low metabolic rates44 and their capability to feed on particulate and dissolved organic matter45 should buffer them against reduced food supply (but see ref. 19).

Temperature-related mechanisms of size change

As temperatures rise, organisms tend to get smaller, a pattern broadly known as the temperature–size rule that is widespread in marine ectotherms46. In general, organisms tend to have higher metabolic rates, faster growth, and mature earlier in the tropics than those in polar regions, which in turn have longer lifespans often leading to larger final size47,48. Modern marine bivalves also show the common pattern of increasing lifespan and decreasing growth rates with latitude (a proxy for temperature)49, but at large do not follow Bergmann’s rule (the assertion that body size increases with latitude)50. This lack of a broadly generalizable latitudinal size gradient within and across bivalve taxa is explained by opposing trends in lifespan and growth rate with latitude that cancel each other out49. Still, we can expect within-species size reductions during episodes of warming at any given latitude if populations shift toward the upper thermal limits of their thermal niche. Of central importance for the performance of organisms with temperatures rising beyond their thermal optimum is that they maintain the scope for aerobic activity in spite of increasing oxygen demand6,51. Once the mismatch between oxygen supply capacity and oxygen demand exceeds a critical threshold, physiological functions are affected negatively, leading, amongst other effects, to reduced growth and finally mortality52.

Our results, however, suggest only minor size reductions within some bivalve species limited to the beginning and the end of the hot TOAE interval (Fig. 4). These somewhat lowered size values might have a small cumulative effect in reducing community level shell size during the TOAE but cannot explain the magnitude of the actual size reductions. Rather, many bivalve species present before and after the TOAE were rare during the TOAE, and changes in species composition are even stronger in brachiopods (Figs. 2 and 4). Apparently, the local populations were not generally able to adapt to the persistently warmer temperatures and any related changes that existed during the TOAE interval.

Thus, the primary mechanism of size change in the studied bivalve and brachiopod communities are variations in species composition (Figs. 2 and 4) and in the relative abundance of differently sized species, with smaller species prevailing during the TOAE (Fig. 5, Supplementary Fig. S3). Specifically, the size decline during the TOAE is paralleled by relative abundance declines in larger-sized species, and both ecological variables are significantly correlated with bottom water temperatures as deduced from the oxygen isotope record (Table 2). Changes in community composition and species abundance are not only compatible with the observed lag 0 correlations but also with the lag 1 correlations that indicate an effect with a brief temporal offset between changes in water temperature and subsequent changes in community shell size. Greater susceptibility of larger versus smaller aquatic ectotherms is known from modern marine ecosystems. Locally, loss of larger specimens of a species occurs first, followed by enhanced mortality, decline in reproduction rates, and local extinctions53,54. Meta-analyses of extant aquatic ectotherms showed a significant increase in the proportion of small-sized species in warming oceans1, and a more negative temperature–size relationship in larger than smaller species47. Again, higher oxygen requirements in larger organisms have been proposed to explain this difference in short-term responses to warming47,53, but other factors such as energy balance may have become important in the long-term54.

Variable response of bivalves and brachiopods to warming

The size response of bivalves and brachiopods to temperature change appears to be decoupled at the onset of the warming phase (Fig. 3). Bivalves show a strong temperature-size correlation (Table 2). They did not experience unusually intense extirpations (Fig. 2) but warming affected larger-sized species more negatively than smaller-sized species. Physiological experiments have shown that molluscs are amongst the most tolerant invertebrate groups towards increased temperatures (summarized in ref. 5), presumably because they tend to be more active organisms that have a higher aerobic scope to meet increased oxygen demands at raised temperatures54,55 than, for example, sessile brachiopods. This is consistent with our data: despite size-specific changes in species composition and abundance during the warm TOAE interval, most bivalve species ranged through the TOAE (Fig. 2).

Conversely, the brachiopods thriving before the TOAE disappeared completely during the early warming phase (Fig. 2). None of the pre-TOAE articulate brachiopod species of the Iberian platform system survived this episode24. In contrast to bivalves, shell size of brachiopod-subcommunities remained stable during the distinct temperature rise in the early phase of the TOAE (Fig. 3), a pattern also reported from other parts of the Iberian Range24. The shift to smaller sizes in the upper part of the TOAE hyperthermal is entirely due to the appearance of a smaller-sized brachiopod species, the basiliolid Soaresirhynchia bouchardi, at the concurrent absence of larger-sized brachiopod species (Figs. 2 and 4 and Supplementary Fig. S3).

Information on the thermal tolerance of brachiopods is scarce, and it is thus difficult to predict their response to warming. Available evidence from the Antarctic rhynchonellid Liothyrella uva points at lower thermal tolerance of this species compared to bivalves from the same environment56. Despite the absence of a significant correlation between shell size and temperature for brachiopods across the whole studied time interval (Table 2), brachiopod turnover and extinctions in the early part of the TOAE hyperthermal suggest that they reacted more sensitively to heat stress than bivalves, conforming to the observations of ref. 56. Furthermore, the high abundances of the relatively small-sized Soaresirhynchia bouchardi in the later part of the TOAE are noteworthy (Fig. 4). It is regarded as a slow-growing species of deeper water origin belonging to a group that migrated into shallow shelf settings during the environmental perturbations of the TOAE, and that succeeded by opportunistically exploiting the ecological space left unoccupied after the extinction of the pre-existing brachiopod fauna32,57. Reduced size suggests reduced metabolic rates, which makes organisms like S. bouchardi more tolerant against increasing temperatures (and other environmental stressors) than larger-sized organisms with higher metabolic demands58. We suggest that also the shift in brachiopod composition in the TOAE interval towards populations of relatively small-sized S. bouchardi was a consequence of concomitant temperature stress. With regard to anthropogenic climate warming and its ecological effects on marine life in the near future, a similar proliferation of relatively small-sized immigrants and long-term reductions in community size structure are worrying perspectives.

Conclusions

We find strong evidence that shell size of macrobenthic communities at Barranco de la Cañada was overall smaller during the environmental crisis represented by the TOAE than before and afterwards. Rather than size change within individual species the key mechanism of size reduction was a decline in the presence and abundance of larger-sized species.

While low oxygen conditions can be excluded as a main driver of shell size reductions in the well oxygenated environments studied herein, we show that temperature correlates negatively particularly with the average shell size of bivalve subcommunities and with the percentage of larger-sized bivalves. Also, for brachiopods, albeit not supported statistically in the temperature–size time series correlation, we argue that extinction-related turnover and the success of a smaller-sized disaster species during the crisis are best explained by seawater warming. Obviously, the nature of environmental stresses varied geographically and it remains unclear at present to which degree additional drivers such as ocean acidification, and altered nutrient regimes may have influenced the observed faunal patterns. We conclude that the long-standing paradigm of severe oxygen restrictions as the main cause of faunal change during the TOAE needs to be modified by including heat stress as an important environmental factor.

Methods

Sampled material and databases

We performed quantitative bed-by-bed sampling from carbonate beds and we standardized sampling intensity by consistently collecting ~13 kg of bulk rock for each sample. Sampling focused on the complete coverage of shelly benthic macroinvertebrates, regardless of preservation quality and without preferential extraction of smaller or larger specimens. Specimens were identified at species level as far as preservation quality allowed.

We recorded dorsal valves, ventral valves, and double-valved specimens for brachiopods and left, right, and articulated valves for bivalves. Measurements were inferred when a small fraction of the shell was missing, while unidentifiable and strongly fragmented specimens were disregarded. Each specimen was considered as one individual, after confirming that the shell sizes of right and left valves of the same species in any sample were different and therefore did not stem from the same individual. Sampling yielded a total of 3,668 occurrences of 93 taxa (62 bivalves, 21 brachiopods, 9 gastropods and 1 coral) (Fig. 2). Because gastropods and corals are rare and fragmented we excluded them from all quantitative analyses.

We performed our analyses on two types of data, quantitative faunal data (shell size) and geochemical data (oxygen isotopes). The shell size dataset is composed of the measurements taken in the field and/or after preparation with digital calipers to the nearest 0.1 mm, accounting for 2,408 measured specimens of bivalves and brachiopods. To estimate the size of communities as a whole we assigned a size value also to specimens for which no direct size measurements were available. These size values were calculated as the mean size of the species in the respective sample. If no measurements were available for a species in a sample we used the mean size of that species in the samples directly above and below. The few taxa with insufficient size data were deleted. The final dataset is composed of 3,433 specimens of bivalves and brachiopods, of which 30% of the measurements were inferred indirectly. To evaluate whether this procedure influenced our analytical outcome we compared our results with those obtained from using just the actually measured specimens. Both analyses yielded congruent size patterns and statistical results. Specimens collected in the field are deposited at the Museo de Ciencias Naturales de Universidad de Zaragoza (ref. 59; inventory numbers MPZ 2019/415 – MPZ 2019/571, MPZ 2019/792 – MPZ 2019/889, MPZ 2019/920 – MPZ 2019/942 and MPZ 2019/1041).

Isotope data

Detailed description of sampling routines, and assessment of fossil preservation and validity of geochemical signatures for palaeoenvironmental interpretation are presented in ref. 32. In brief, fossil shell material was extracted after removal of any altered crusts and sediment using a preparation needle or scalpel. For brachiopods fibrous, secondary shell layer material was outlined with the preparation needle and levered off the shell with the needle checking for any possible contamination with altered material or bulk rock matrix. Only visually clean and well-preserved material was accepted for further analysis. Gryphaea material was treated in the same way, but where the shell was compact and too hard for efficient use of a preparation needle, a scalpel was employed to shave off shell calcite from the fossil surface. Typically, a few milligrams of calcite were stored in individual containers for further geochemical analysis. Time averaging as a function of sample size and ontogeny is known to affect the amplitude of sclerochronological proxy signals60. In order to minimize biases resulting from widely different shell quantities, a target sample size of 4 mg was chosen, which allowed to replicate measurements in case one or several analyses would have failed. Oyster shell increments were typically extracted from comparatively wide areas crossing as few as possible growth increments. For brachiopods shell material was taken parallel to the orientation of shell fibres, and therefore somewhat oblique to growth direction, which may have led to some dampening of seasonal signals extracted from these shells. The observed isotopic variability within individual fossils of typically about 1 permil suggests that resolution of the data is generally significantly higher than yearly. However, in the absence of clear morphological markers of growth rate, the exact time increments covered by single samples cannot be estimated precisely.

Approximately 500 µg of calcite were taken for C and O isotope analysis using the Sercon 20–22 gas source isotope ratio mass spectrometer at the University of Exeter’s Penryn campus employing the continuous flow technique. The calcite material was put into borosilicate glass containers, sealed with rubber septa, and flushed with He for 80 s to remove atmospheric contaminants. After subsequent manual injection of c 100 µL of nominally anhydrous H3PO4 and reaction at 70 °C, the samples were measured together with two in-house isotope standards (CAR, Carrara Marble; NCA, Namibian Carbonatite), allowing for correction for instrumental drift and biases. Reproducibility of the measurements was controlled by the results of CAR and was found to be ± 0.07‰ (2 sd) for δ13C and ± 0.15‰ (2 sd) for δ18O, both for the standard analyses in conjunction with studied samples (n = 125) and for the entire year 2018 (n = 917).

To control ultrastructure preservation, a fragment of shell from each studied fossil specimen was also submitted to scanning electron microscope analysis using a FEI Quanta 650 Field Emission Gun SEM at the University of Exeter’s Penryn Campus. For further quantification of shell preservation, about 500 µg of calcite per sample were analysed for element/Ca ratios using an Agilent 5110 VDV ICP-OES at the University of Exeter’s Penryn Campus. Ultrastructure preservation of the shell material was found to be mostly very good to excellent, with brachiopod samples showing only minor features of surficial shell dissolution but lack of neomorphic calcite and recrystallization. Samples exceeding Mn/Ca ratios of 0.1 mmol/mol and/or Fe/Ca ratios of 1 mmol/mol were rejected from further interpretation. Isotopic signals were tested for taxonomic effects and potential metabolic effects to ensure that compositional changes of fossil assemblages did not lead to biased interpretation. Both oysters and secondary shell layer calcite of rhynchonellid brachiopods are thought to represent excellent substrates for palaeotemperature extraction for the Mesozoic essentially devoid of vital effects61,62. Differences between brachiopods and Gryphaea as well as individuals of different brachiopod taxa in our dataset were undistinguishable from differences between individuals of a single taxon, leading us to conclude that inter-species bias and vital effects can be ignored for the present dataset.

Carbon isotope ratios of the studied specimens were used solely to constrain the extent of the well-known, large, Early Toarcian negative carbon isotope excursion (e.g., ref. 63), confirming ammonite biostratigraphy and increasing stratigraphic resolution of the dataset.

Palaeotemperatures were derived from oxygen isotope ratios of samples that passed screening for alteration and were computed using the brachiopod-specific oxygen thermometer of ref. 35:

$${\rm{T}}\,^\circ {\rm{C}}=16.192-3.468\ast ({\delta }^{18}{{\rm{O}}}_{{\rm{calcite}}}-{\delta }^{18}{{\rm{O}}}_{{\rm{seawater}}}-{{\rm{Mg}}}_{{\rm{calcite}}})$$

using an average MgCO3 content of 0.4 wt% of the fossil shell calcite which has minimal effects on the resulting temperature. Like all other conventional oxygen isotope thermometers this equation requires an estimate of ambient water composition which we set at −1‰ V-SMOW in line with other work published for the studied area and time interval (e.g., ref. 64). For the derivation of relative temperature change as pictured in the present study the ambient water composition, however, is irrelevant as long as it did not change substantially across the studied interval, because the sensitivity of the oxygen thermometer of ref. 35 is constant. Salinity changes as major driver of the isotopic signal were discounted (see Discussion).

Statistical methods

Shell size is calculated as the log2 of the geometric mean of two dimensions. The geometric mean was determined using the following formulae65, where L = shell length, W = shell width and H = shell height:

$${{\rm{GeoMean}}}_{{\rm{Brachiopods}}}=\sqrt{{\rm{L}}\ast {\rm{W}}}\,{\rm{and}}\,{{\rm{GeoMean}}}_{{\rm{Bivalves}}}=\sqrt{{\rm{L}}\ast {\rm{H}}}$$

Shell size analyses for the brachiopod subcommunities were performed on articulate brachiopods only.

Calculating the percentage of larger-sized individuals per sample is based on the common species only, i.e. those that occur with at least three specimens per level and at at least three sampling levels. We calculated the mean shell size of each of these common species and species where classified as either smaller- or larger-sized by using as a cut-off the global mean of the individual species’ mean shell size (Supplementary Fig. S2). The relative abundance of individuals of larger-sized species per sample, expressed as percentage relative to the total count of individuals of common species in each sample, was calculated and the trajectory fitted with a three-point moving average.

Correlation tests

Before determining the degree of correlation between δ18O values with shell size and with the percentage of larger-sized individuals through time, we deleted the rows with missing values in any of the two time series.

The following steps were performed before the Generalized Least Square (GLS) regression (gls function in “nlme” package66), the results of which are summarized in Supplementary Tables S1S4: (i) the presence of any trend in time was investigated for each time series (shell size/percentage of larger-sized individuals ~ sampling level, and δ18O ~ sampling level) through a simple Ordinary Least Squares (OLS) regression and with a Spearman’s Rank correlation test for a comparison; (ii) we checked for autocorrelation and partial autocorrelation of the relationships shell size/percentage of larger-sized individuals ~ δ18O through the acf function in base R and durbinWatsonTest function from the “car” package67. The original time series were kept for further analyses in cases of non-significant p-values from step (i) and/or no serious autocorrelation issues from step (ii); otherwise the time series was detrended via generalized differencing68 with the R script available at ‘http://www.graemetlloyd.com/pubdata/functions_2.r’; (iii) we fitted an ARIMA process with the auto.arima function in the “forecast” R package69,70 to the residuals from OLS regression of shell size/percentage of larger-sized individuals ~ δ18O. Because it is possible that unit roots are present as a different facet of an ARIMA process, the residual series of the fitted ARIMA process was investigated with the ndiffs function from the “forecast” package (with kpss and adf stationarity tests and maximum fifth order differencing applied). Given the negative outcomes of the tests (i.e. no differencing required), we proceeded with the GLS proper; (iv) the ARIMA fit was finally applied in the GLS regression to specify the expected correlation structure of the residuals. All analyses were performed in R (v. 3.5.371).

Data availability

The datasets generated and analysed during the current study are available in the Dryad Digital Repository at https://doi.org/10.5061/dryad.rr4xgxd5v.

References

  1. 1.

    Daufresne, M., Lengfellner, K. & Sommer, U. Global warming benefits the small in aquatic ecosystems. PNAS 106(31), 12788–12793, https://doi.org/10.1073/pnas.0902080106 (2009).

  2. 2.

    Sheridan, J. A. & Bickford, D. Shrinking body size as an ecological response to climate change. Nat. Clim. Change 1, 401–406, https://doi.org/10.1038/NCLIMATE1259 (2011).

  3. 3.

    Reuman, D. C., Holt, R. D. & Yvon-Durocher, G. A metabolic perspective on competition and body size reductions with warming. J. Anim. Ecol. 83, 59–69, https://doi.org/10.1111/1365-2656.12064 (2014).

  4. 4.

    Calosi, P., Putnam, H. M., Twitchett, R. J. & Vermandele, F. Marine metazoan modern mass extinction: Improving predictions by integrating fossil, modern, and physiological data. Annu. Rev. Mar. Sci. 11, 369–390, https://doi.org/10.1146/annurev-marine-010318-095106 (2019).

  5. 5.

    Song, H. et al. Anoxia/high temperature double whammy during the Permian–Triassic marine crisis and its aftermath. Sci. Rep. 4, srep04132, https://doi.org/10.1038/srep04132 (2014).

  6. 6.

    Pörtner, H.-O., Bock, C. & Mark, F. C. Oxygen- and capacity-limited thermal tolerance: bridging ecology and physiology. J. Exp. Bio. 220, 2685–2696, https://doi.org/10.1242/jeb.134585 (2017).

  7. 7.

    Pörtner, H.-O. & Farrell, A. P. Physiology and climate change. Science 322, 690–692, https://doi.org/10.1126/science.ll63156 (2008).

  8. 8.

    Gardner, J. L., Peters, A., Kearney, M. R., Joseph, L. & Heinsohn, R. Declining body size: a third universal response to warming? Trends Ecol. Evol. 26(6), 285–291, https://doi.org/10.1016/j.tree.2011.03.005 (2011).

  9. 9.

    Gienapp, P., Teplitsky, C., Alho, J. S., Mills, J. A. & Merilä, J. Climate change and evolution: disentangling environmental and genetic responses. Mol. Ecol. 17, 167–178, https://doi.org/10.1111/j.1365-294X.2007.03413.x (2008).

  10. 10.

    Pálfy, J. & Smith, P. L. Synchrony between Early Jurassic extinction, oceanic anoxic event, and the Karoo-Ferrar flood basalt volcanism. Geology 28(8), 747–750, 10.1130/0091-7613(2000)028<0747:sbejeo>2.3.co;2 (2000).

  11. 11.

    Morten, S. D. & Twitchett, R. J. Fluctuations in the body size of marine invertebrates through the Pliensbachian–Toarcian extinction event. Palaeogeogr. Palaeoclimatol. Palaeoecol. 284, 29–38, https://doi.org/10.1016/j.palaeo.2009.08.023 (2009).

  12. 12.

    Caswell, B. A. & Coe, A. L. Primary productivity controls on opportunistic bivalves during Early Jurassic oceanic deoxygenation. Geology 41(11), 1163–1166, https://doi.org/10.1130/G34819.1 (2013).

  13. 13.

    Martindale, R. C. & Aberhan, M. Response of macrobenthic communities to the Toarcian Oceanic Anoxic Event in northeastern Panthalassa (Ya Ha Tinda, Alberta, Canada). Palaeogeogr. Palaeoclimatol. Palaeoecol. 478, 103–120, https://doi.org/10.1016/j.palaeo.2017.01.009 (2017).

  14. 14.

    Caswell, B. & Dawn, S. J. Recovery of benthic communities following the Toarcian oceanic anoxic event in the Cleveland Basin, UK. Palaeogeogr. Palaeoclimatol. Palaeoecol. 521, 114–126, https://doi.org/10.1016/j.palaeo.2019.02.014 (2019).

  15. 15.

    Ros-Franch, S. et al. Population response during an Oceanic Anoxic Event: The case of Posidonotis (Bivalvia) from the lower Jurassic of the Neuquén Basin, Argentina. Palaeogeogr. Palaeoclimatol. Palaeoecol. 525, 57–67, https://doi.org/10.1016/j.palaeo.2019.04.009 (2019).

  16. 16.

    Jenkyns, H. C. Geochemistry of oceanic anoxic events. Geochem. Geophys. Geosyst. 11, Q03004, https://doi.org/10.1029/2009GC002788 (2010).

  17. 17.

    Dera, G. & Donnadieu, Y. Modeling evidences for global warming, Arctic seawater freshening, and sluggish oceanic circulation during the Early Toarcian anoxic event. Paleoceanography 27, PA2211, https://doi.org/10.1029/2012PA002283 (2012).

  18. 18.

    Them, T. R. et al. Thallium isotopes reveal protracted anoxia during the Toarcian (Early Jurassic) associated with volcanism, carbon burial, and mass extinction. PNAS 115(26), 6596–6601, https://doi.org/10.1073/pnas.1803478115 (2018).

  19. 19.

    Fürsich, F. T., Berndt, R., Scheuer, T. & Gahr, M. Comparative ecological analysis of Toarcian (Lower Jurassic) benthic faunas from southern France and east-central Spain. Lethaia 34, 169–199, https://doi.org/10.1111/j.1502-3931.2001.tb00048.x (2001).

  20. 20.

    Gómez, J. J. & Goy, A. Warming-driven mass extinction in the Early Toarcian (Early Jurassic) of northern and central Spain. Correlation with other time-equivalent European sections. Palaeogeogr. Palaeoclimatol. Palaeoecol. 306, 176–195, https://doi.org/10.1016/j.palaeo.2011.04.018 (2011).

  21. 21.

    García Joral, F., Baeza-Carratalá, J. F. & Goy, A. Changes in brachiopod body size prior to the Early Toarcian (Jurassic) mass extinction. Palaeogeogr. Palaeoclimatol. Palaeoecol. 506, 242–249, https://doi.org/10.1016/j.palaeo.2018.06.045 (2018).

  22. 22.

    Piazza, V., Duarte, L. V., Renaudie, J. & Aberhan, M. Reductions in body size of benthic macroinvertebrates as a precursor of the early Toarcian (Early Jurassic) extinction event in the Lusitanian Basin, Portugal. Paleobiology 45(2), 296–316, https://doi.org/10.1017/pab.2019.11 (2019).

  23. 23.

    Ruvalcaba Baroni, I. et al. Ocean circulation in the Toarcian (Early Jurassic): A key control on deoxygenation and carbon burial on the European shelf. Paleoceanography and Paleoclimatology 33, 994–1012, https://doi.org/10.1029/2018PA003394 (2018).

  24. 24.

    García Joral, F., Gómez, J. J. & Goy, A. Mass extinction and recovery of the Early Toarcian (Early Jurassic) brachiopods linked to climate change in Northern and Central Spain. Palaeogeogr. Palaeoclimatol. Palaeoecol. 302, 367–380, https://doi.org/10.1016/j.palaeo.2011.01.023 (2011).

  25. 25.

    Danise, S., Twitchett, R. J. & Little, C. T. S. Environmental controls on Jurassic marine ecosystems during global warming. Geology 43(3), 263–266, https://doi.org/10.1130/G36390.1 (2015).

  26. 26.

    Danise, S. et al. Stratigraphic and environmental control on marine benthic community change through the early Toarcian extinction event (Iberian Range, Spain). Palaeogeogr. Palaeoclimatol. Palaeoecol. 524, 183–200, https://doi.org/10.1016/j.palaeo.2019.03.039 (2019).

  27. 27.

    Goy, A., Gómez, J. J. & Yébenes, A. El Jurásico de la Rama Castellana de la Cordillera Ibérica (Mitad Norte). Est. Geol. 32, 391–423 (1976).

  28. 28.

    Gahr, M. E. Palökologie des Makrobenthos aus dem Unter-Toarc SW-Europas. Beringeria 31, 3–204 (2002).

  29. 29.

    Gahr, M. E. Response of Lower Toarcian (Lower Jurassic) macrobenthos of the Iberian Peninsula to sea level changes and mass extinction. J. Iberian Geol. 31(2), 197–215 (2005).

  30. 30.

    Gómez, J. J. & Goy, A. Late Triassic and Early Jurassic palaeogeographic evolution and depositional cycles of the Western Tethys Iberian platform system (Eastern Spain). Palaeogeogr. Palaeoclimatol. Palaeoecol. 222, 77–94, https://doi.org/10.1016/j.palaeo.2005.03.010 (2005).

  31. 31.

    García Joral, F. & Goy, A. Rhynchonellida (Brachiopoda) Biozones of the Toarcian in the Iberian and Cantabrian Cordilleras (Spain) in Comunicaciones del V Congreso del Jurásico de España (eds. Ruiz-Omeñaca, J. I., Piñuela, L. & García-Ramos, J. C.) 3–9 (Museo del Jurásico de Asturias, Colunga (2010).

  32. 32.

    Ullmann, C. V. et al. Warm afterglow from the Toarcian Oceanic Anoxic Event drives the success of deep-adapted brachiopods. (revised ms submitted to Sci. Rep.).

  33. 33.

    Aurell, M. et al. Transgressive–regressive cycles and Jurassic palaeogeography of northeast Iberia. Sediment. Geol. 162, 239–271, https://doi.org/10.1016/S0037-0738(03)00154-4 (2003).

  34. 34.

    Fürsich, F. T. Palaeoecology and evolution of Mesozoic salinity-controlled benthic macroinvertebrate associations. Lethaia 26, 327–346 (1994).

  35. 35.

    Brand, U. et al. Oxygen isotopes and MgCO3 in brachiopod calcite and a new paleotemperature equation. Chem. Geol. 359, 23–31, https://doi.org/10.1016/j.chemgeo.2013.09.014 (2013).

  36. 36.

    McArthur, J. M., Algeo, T. J., van de Schootbrugge, B., Li, Q. & Howarth, R. J. Basinal restriction, black shales, Re-Os dating, and the Early Toarcian (Jurassic) oceanic anoxic event. Paleoceanography 23, PA4217, https://doi.org/10.1029/2008PA001607 (2008).

  37. 37.

    Harazim, D. A. et al. Spatial variability of watermass conditions within the European Epicontinental Seaway during the Early Jurassic (Pliensbachian–Toarcian). Sedimentology 60, 359–390, https://doi.org/10.1111/j.1365-3091.2012.01344.x (2013).

  38. 38.

    Korte, C. et al. Jurassic climate mode governed by ocean gateway. Nat. Comm. 6, 10015, https://doi.org/10.1038/ncomms10015 (2015).

  39. 39.

    Thierry, J. et al. Middle Toarcian in Atlas Peri-Tethys Paleogeographical Maps (eds. Dercourt, J. et al.) 1–97 (Paris (2000).

  40. 40.

    van der Veer, G., Voerkelius, S., Lorentz, G., Heiss, G. & Hoogewerff, J. A. Spatial interpolation of the deuterium and oxygen-18 composition of global precipitation using temperature as ancillary variable. J. Geochem. Explor. 101(2), 175–184, https://doi.org/10.1016/j.gexplo.2008.06.008 (2009).

  41. 41.

    Vaquer-Sunyer, R. & Duarte, C. M. Thresholds of hypoxia for marine biodiversity. PNAS 105(40), 15452–15457, https://doi.org/10.1073/pnas.0803833105 (2008).

  42. 42.

    Parker, L. M. et al. Predicting the response of molluscs to the impact of ocean acidification. Biology 2, 651–692, https://doi.org/10.3390/biology2020651 (2013).

  43. 43.

    Cross, E. L., Harper, E. M. & Peck, L. S. A 120-year record of resilience to environmental change in brachiopods. Glob. Change Biol. 24, 2262–2271, https://doi.org/10.1111/gcb.14085 (2018).

  44. 44.

    Peck, L. S. & Harper, E. M. Variation in size of living articulated brachiopods with latitude and depth. Mar. Biol. 157, 2205–2213, https://doi.org/10.1007/s00227-010-1486-5 (2010).

  45. 45.

    Steele-Petrović, H. M. Brachiopod food and feeding processes. Palaeontology 19, 417–436 (1976).

  46. 46.

    Audzijonyte, A. et al. Is oxygen limitation in warming waters a valid mechanism to explain decreased body sizes in aquatic ectotherms? Glob. Ecol. Biogeogr. 28, 64–77, https://doi.org/10.1111/geb.12847 (2019).

  47. 47.

    Forster, J., Hirst, A. G. & Atkinson, D. Warming-induced reductions in body size are greater in aquatic than terrestrial species. PNAS 109(47), 19310–19314, https://doi.org/10.1073/pnas.1210460109 (2012).

  48. 48.

    Verberk, W. C. E. P. & Atkinson, D. Why polar gigantism and Palaeozoic gigantism are not equivalent: effects of oxygen and temperature on the body size of ectotherms. Funct. Ecol. 27, 1275–1285, https://doi.org/10.1111/1365-2435.12152 (2013).

  49. 49.

    Moss, D. K. et al. Lifespan, growth rate, and body size across latitude in marine Bivalvia, with implications for Phanerozoic evolution. Proc. R. Soc. B 283, 20161364, https://doi.org/10.1098/rspb.2016.1364 (2016).

  50. 50.

    Berke, S. K., Jablonski, D., Krug, A. Z., Roy, K. & Tomasovych, A. Beyond Bergmann’s rule: size–latitude relationships in marine Bivalvia world-wide. Glob. Ecol. Biogeogr. 22, 173–183, https://doi.org/10.1111/j.1466-8238.2012.00775.x (2013).

  51. 51.

    Atkinson, D., Morley, S. A. & Hughes, R. N. From cells to colonies: At what levels of body organization does the ‘temperature-size rule’ apply? Evol. Dev. 8(2), 202–214, https://doi.org/10.1111/j.1525-142X.2006.00090.x (2006).

  52. 52.

    Pörtner, H.-O. Climate dependent evolution of Antarctic ectotherms: an integrative analysis. Deep-Sea Res. II 53(8-10), 1071–1104, https://doi.org/10.1016/j.dsr2.2006.02.015 (2006).

  53. 53.

    Pörtner, H.-O. & Knust, R. Climate Change Affects Marine Fishes Through the Oxygen Limitation of Thermal Tolerance. Science 315(5808), 95–97, https://doi.org/10.1126/science.1135471 (2017).

  54. 54.

    Peck, L. S., Clark, M. S., Morley, S. A., Massey, A. L. & Rossetti, H. Animal temperature limits and ecological relevance: effects of size, activity and rates of change. Funct. Ecol. 23, 248–256, https://doi.org/10.1111/j.1365-2435.2008.01537.x (2009).

  55. 55.

    Pörtner, H.-O. Oxygen- and capacity-limitation of thermal tolerance: a matrix for integrating climate-related stressor effects in marine ecosystems. J. Exp. Biol. 213, 881–893, https://doi.org/10.1242/jeb.037523 (2010).

  56. 56.

    Clark, M. S. et al. Biodiversity in marine invertebrate responses to acute warming revealed by a comparative multi-omics approach. Glob. Chang. Biol. 23, 318–330, https://doi.org/10.1111/gcb.13357 (2017).

  57. 57.

    Vörös, A. The smooth brachiopods of the Mediterranean Jurassic: Refugees or invaders? Palaeogeogr. Palaeoclimatol. Palaeoecol. 223, 222–242, https://doi.org/10.1016/j.palaeo.2005.04.006 (2005).

  58. 58.

    Payne, J. L., Heim, N. A., Knope, M. L. & McClain, C. R. Metabolic dominance of bivalves predates brachiopod diversity decline by more than 150 million years. Proc. R. Soc. Lond. B 281, 20133122, https://doi.org/10.1098/rspb.2013.3122 (2014).

  59. 59.

    Canudo, J. I. The collection of type fossils of the Natural Science Museum of the University of Zaragoza (Spain). Geoheritage 10, 385–392, https://doi.org/10.1007/s12371-017-0228-1 (2018).

  60. 60.

    Schöne, B. R. & Fiebig, J. Seasonality in the North Sea during the Allerød and Late Medieval climate optimum using bivalve sclerochronology. Int. J. Earth Sci. 98(1), 83–98, https://doi.org/10.1007/s00531-008-0363-7 (2009).

  61. 61.

    Ullmann, C. V., Wiechert, U. & Korte, C. Oxygen isotope fluctuations in a modern North Sea oyster (Crassostrea gigas) compared with annual variations in seawater temperature: Implications for palaeoclimate studies. Chem. Geol. 277(1-2), 160–166, https://doi.org/10.1016/j.chemgeo.2010.07.019 (2010).

  62. 62.

    Ullmann, C. V., Frei, R., Korte, C. & Lüter, C. Element/Ca, C and O isotope ratios in modern brachiopods: Species-specific signals of biomineralization. Chem. Geol. 460, 15–24, https://doi.org/10.1016/j.chemgeo.2017.03.034 (2017).

  63. 63.

    Hesselbo, S. P., Jenkyns, H. C., Duarte, L. V. & Oliveira, L. C. V. Carbon-isotope record of the Early Jurassic (Toarcian) Oceanic Anoxic Event from fossil wood and marine carbonate (Lusitanian Basin, Portugal). Earth Planet. Sci. Lett. 253, 455–470, https://doi.org/10.1016/j.epsl.2006.11.009 (2007).

  64. 64.

    Suan, G., Mattioli, E., Pittet, B., Mailliot, S. & Lécuyer, C. Evidence for major environmental perturbation prior to and during the Toarcian (Early Jurassic) oceanic anoxic event from the Lusitanian Basin, Portugal. Paleoceanography 23, PA1202, https://doi.org/10.1029/2007PA001459 (2008).

  65. 65.

    Kosnik, M. A., Jablonski, D., Lockwood, R. & Novack-Gottshall, P. M. Quantifying molluscan body size in evolutionary and ecological analyses: maximizing the return on data-collection efforts. Palaios 21(6), 588–597, https://doi.org/10.2110/palo.2006.p06-012r (2006).

  66. 66.

    Pinheiro, J., Bates, D., DebRoy, S., Sarkar, D. and R Core Team. nlme: Linear and Nonlinear Mixed Effects Models. R package version 3.1–137: https://CRAN.R-project.org/package=nlme (2018).

  67. 67.

    Fox, J. & Weisberg, S. An {R} Companion to Applied Regression, Second Edition. Thousand Oaks CA: Sage: http://socserv.socsci.mcmaster.ca/jfox/Books/Companion (2011).

  68. 68.

    McKinney, M. L. Classifying and analyzing evolutionary trends in Evolutionary trends (ed. McNamara, K. J.) 28–58 (Tucson, University of Arizona Press (1990).

  69. 69.

    Hyndman, R. J. & Khandakar, Y. Automatic time series forecasting: the forecast package for R. J. Stat. Soft. 26(3), 1–22, http://www.jstatsoft.org/article/view/v027i03 (2008).

  70. 70.

    Hyndman, R. et al. forecast: Forecasting functions for time series and linear models. R package version 8.5, http://pkg.robjhyndman.com/forecast (2019).

  71. 71.

    R Core Team. R: A language and environment for statistical computing. R Foundation for Statistical Computing, Vienna, Austria, https://www.R-project.org/ (2019).

Download references

Acknowledgements

Tina Klein and Friedrich Lucassen (Center for Marine Environmental Sciences, University of Bremen) are warmly thanked for joint fieldwork, Adam Kocsis and Carl Reddin (University of Erlangen) for advice on statistical methods, and Wolfgang Kiessling (University of Erlangen), David Lazarus (Museum für Naturkunde) and Will Foster (University College Dublin) for their suggestions for improvements of the manuscript. The manuscript benefitted substantially by the constructive feedback provided by Seth Finnegan and an anonymous reviewer. This study was funded by the Deutsche Forschungsgemeinschaft grant DFG AB 09/10-1 and is part of the Research Unit TERSANE (FOR 2332: Temperature‐related Stressors as a Unifying Principle in Ancient Extinctions). This work is also a contribution to the IGCP-655 (IUGS-UNESCO: Toarcian Oceanic Anoxic Event: Impact on Marine Carbon Cycle and Ecosystems). We thank Juan Carlos García and the Dirección General de Cultura y Patrimonio (Gobierno de Aragon, Zaragoza) for authorizing field work and José Ignacio Canudo (Universidad de Zaragoza) for the loan of specimens. C.V.U acknowledges funding from the UK Natural Environment Research Council (NE/N018508/1).

Author information

V.P. and M.A. developed the idea of the presented study. V.P. took part in fieldwork, identified the specimens, analysed the data, wrote the manuscript and prepared all figures and tables. M.A. participated in fieldwork, assisted with taxonomical identification, and contributed to the writing of the manuscript. C.V.U. provided the geochemical data and contributed to the writing of part of manuscript. All authors reviewed the manuscript.

Correspondence to Veronica Piazza or Martin Aberhan.

Ethics declarations

Competing interests

The authors declare no competing interests.

Additional information

Publisher’s note Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.

Supplementary information

Rights and permissions

Open Access This article is licensed under a Creative Commons Attribution 4.0 International License, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the article’s Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder. To view a copy of this license, visit http://creativecommons.org/licenses/by/4.0/.

Reprints and Permissions

About this article

Verify currency and authenticity via CrossMark

Cite this article

Piazza, V., Ullmann, C. & Aberhan, M. Temperature-related body size change of marine benthic macroinvertebrates across the Early Toarcian Anoxic Event. Sci Rep 10, 4675 (2020). https://doi.org/10.1038/s41598-020-61393-5

Download citation

Comments

By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.