Supplementary Information For

Home , Anderdon Limestone, Arenig, Berriasian, Callovian, Darriwilian

Supplementary Information for

Asteroid break-ups and meteorite delivery to Earth the past 500 million years

Fredrik Terfelt and Birger Schmitz

Corresponding author: Birger Schmitz

Email: [email protected]

This PDF file includes:

Supplementary Text

Figures S1 to S5

Tables S1 to S2

Legend for Dataset S1

SI References

Other supplementary materials for this manuscript include the following:

Dataset S1

1 Supplementary Text

Geological setting

The mid-to-late Cambrian of Scandinavia. The Drumian and Guzhangian stages in Scandinavia are part of the Alum Shale Formation, dominated by kerogen-rich black shales with a few organic-rich limestone beds. The condensed alum shales and limestone beds formed ~506 – 478 Ma ago when Scandinavia was covered by a shallow epicontinental sea on a peneplained passive margin of the Baltic shield (1-4). As such, sedimentation rates were extremely low and Scandinavia was tectonically undisturbed for a substantial amount of time. The Hypagnostus Limestone bed of the Drumian Stage is developed as an approximately 60 cm thick, organic-rich, massive limestone succession in Västergötland, south-central Sweden. It belongs to the uppermost part of the Ptychagnostus atavus global agnostoid Zone correlating to the uppermost Hypagnostus parvifrons regional agnostoid Zone in Scandinavia. In Scania, southernmost Sweden, the corresponding level is developed as shale (4). The Andrarum Limestone bed of the Guzhangian Stage is developed as an approximately 1 meter thick, massive limestone bed in Scania, southernmost Sweden. It belongs to the Lejopyge laevigata global agnostoid Zone and correlates to the Solenopleura brachymetopa regional polymerid Zone in Scandinavia. In Västergötland, the corresponding level is developed as a conglomerate (the Exporrecta Conglomerate) (4).

The Middle Jurassic of north-eastern Italy. The upper Bajocian to the Tithonian of the Altipiano de Asiago area is represented by red pelagic limestones colloquially referred to as the Rosso Ammonitico Veronese (5). This succession is divided into three units; the lower, middle and upper Ammonitico Rosso. The lower Ammonitico Rosso comprises upper Bajocian to lower Callovian strata and our samples derive from the lower Bathonian part of this succession in the Asiago section, outside the city of Asiago.

The mid-to-late Jurassic of southern Spain. The middle to early Jurassic in southern Spain is represented by a shallow inner shelf carbonate platform situated at the South Iberian paleomargin. The platform underwent emersion, erosion and a subsequent formation of hydromorphic soils (6). As such, a discontinuity surface representing Late Bathonian to Middle Oxfordian strata, sits at the base of Middle Oxfordian limestones (6). Following drowning in Middle Oxfordian times, sponge meadows thrived, which resulted in spongiolithic limestones in the Middle-Upper Oxfordian (6).

The samples processed in this study consist of red-coloured limestones from the transition zone just below the erosion surface below the middle Oxfordian strata at the Carcabuey section, province of Córdoba. Consequently, our sampled 0.4 m of strata represents 2.5-5.5 million years.

Variables affecting the flux of extraterrestrial chrome spinel

In our first-order reconstruction of the extraterrestrial flux in the Phanerozoic, three parameters are constants (the density of limestone, the area of deposition and the time), whereas the other two (grain concentration and sedimentation rate) are variables. The density of limestone differs somewhat depending on porosity and impurities in the range of 2.3-2.7 g/cm3 in different settings (7). In this study, the average value of 2.5 g/cm3 is used throughout. Many uncertainties are associated with sedimentation rate estimates in deep time. Non-deposition and erosion are two examples of these uncertainties. Thus, the sedimentation rate is the most uncertain parameter in our flux estimates, however, even large errors in the published rate estimates would not affect the outcome of our results (See Table S2 for an overview of flux variables).

Fig. S1. a, Early Paleocene (66-61 Ma ago, Danian Stage), Bottaccione section, Umbrian Apennines, central Italy. b, Late Cretaceous (92-91 Ma ago, Turonian Stage), Bottaccione section, Umbrian Apennines, central Italy. c, Late Cretaceous (94-92 Ma ago, Cenomanian-Turonian stages), Bottaccione section, Umbrian Apennines, central Italy. d, Early Cretaceous (117-103 Ma ago, Aptian-Albian stages), Pacifica section, California, USA. e, Early Cretaceous (145-133 Ma ago, Berriasian-Hauterivian stages), Monte Acuto and Bosso sections, Apennines, central Italy. f, Middle Jurassic (166-164 Ma ago, Callovian Stage), Carcabuey section, Betic Cordillera, southern Spain. g, Middle Jurassic (168-166 Ma ago, Bathonian Stage), Altopiano de Asiago, northeastern Italy. h, Late Devonian (374-372 Ma ago, Frasnian-Famennian stages), Coumiac section, Montagne Noir, southern France. i, Late Silurian (426- 424 Ma ago, Gorstian-Ludfordian stages), Cellon section, Central Carnic Alps, southern Austria. j, Middle Ordovician (463-462 Ma ago, Darriwilian Stage), Gärde Quarry, Jämtland, central Sweden. k, Middle Ordovician (466-465 Ma ago, Darriwilian Stage), Komstad quarry, Scania, southernmost Sweden. l, Middle Ordovician (467-466 Ma ago, Darriwilian Stage), Lynna river section, western Russia. m, Middle Ordovician (467-466 Ma ago, Darriwilian Stage), Hällekis section, Västergötland, southern Sweden. n, Late Cambrian (500-499 Ma ago, Guzhangian Stage), Andrarum quarry and Baskemölla sections, Scania, southernmost Sweden. o, Late Cambrian (503-502 Ma ago, Drumian Stage), Gudhem quarry, Västergötland, southern Sweden. p, Middle Ordovician (467-465 Ma ago, Darriwilian Stage), Puxi river section, Hubei province, China [this window is not included in the flux calculations, but is a crucial data set showing the reproducibility of the chrome-spinel approach (8)].

Fig. S2. Sampled localities, stratigraphy and outcrops for the Cambrian windows. A, Map over southern Sweden showing the three localities sampled for this study. The Hypagnostus Limestone was sampled from the Gudhem quarry outside the city of Falköping. The Andrarum Limestone was sampled from the Andrarum quarry outside the village of Andrarum and from the Baskemölla beach section at the village of Baskemölla. B, Stratigraphy and composite lithological succession of the Cambrian chrome-spinel yielding units. Encircled A = Andrarum Limestone; encircled H = Hypagnostus Limestone. C, Cored sample from the Andrarum Limestone, Andrarum. D, The Andrarum Limestone in the Baskemölla beach section. Note the 90 degrees overturn of the unit as compared to the same unit in Andrarum. E, Outcrop of the Hypagnostus Limestone (between the dotted lines) in the Gudhem quarry. See SI Supplementary Text for more information.

Fig. S3. Sampled locality, stratigraphy and outcrops for the Bathonian Stage, Italy. A. Map over northeastern Italy showing the location of the Asiago section sampled for this study. B. Stratigraphy and lithologic succession of the Asiago section. C. Overview of the Asiago Quarry. D. Close up of sampled lower-middle portion of the Bathonian Stage in the Asiago section. See SI Supplementary Text for more information.

Fig. S4. Sampled locality, stratigraphy and outcrop for the Callovian Stage, Spain. A. Map over southern Spain showing the location of the Carcabuey section sampled for this study. B. Stratigraphy and lithologic succession for the Carcabuey section. C. Hammer resting on top of the Bathonian- Callovian hardground. D. Preserved ammonite in the hardground. See SI Supplementary Text for more information.

Fig. S5. K-Ar ages of recently fallen ordinary chondrites. A. K-Ar ages of recent H chondrites (9). B. K-Ar ages of recent L chondrites (9). The plots show individual probability distribution for ages of individual meteorites (dashed line) and a combined probability distribution (solid line) for all of the data. The diagrams take in account the uncertainties in the individual data points in a graphical way by giving each data point equal area; see further reference (9). Regarding the more precise timings of impacts on the H-chondrite parent body, see also discussion in reference (10).

Table S1. Phanerozoic flux variation of the groups of ordinary chondrites based on chrome spinel# Time window Ma ago n H (%) L (%) LL (%) (63) Today (11) 0 926§ 41.1 47.4 11.5 Early Paleocene (12) ~66-61 86 69.0 22.0 9.0 Late Cretaceous (13)* ~92-91 113 62.3 28.0 9.7 Late Cretaceous (13) ~94-92 59 49.8 45.1 5.1 Early Cretaceous (14) ~117-103 227 57.4 31.2 11.4 Early Cretaceous (15) ~145-133 81 44.7 44.6 10.7 Middle Jurassic* ~166-164 142 50.8 34.9 14.4 Middle Jurassic* ~168-166 129 51.3 32.3 16.4 Late Devonian (16) ~374-372 112 28.0 59.6 12.3 Late Silurian (17) ~426-424 164 29.8 65.3 4.9 Middle Ordovician (18) ~463-462 23 -4.3 108.7 -4.3 Middle Ordovician (19) ~466-465 119 0.7 101.4 -2.1 Middle Ordovician (15) ~467-466 215 37.6 32.8 29.5 Middle Ordovician (20) ~467-466 243 37.9 32.7 29.3 Late Cambrian* ~500-499 200 71.3 13.4 15.3 Late Cambrian* ~503-502 147 62.0 20.1 17.9

# Based on TiO2 content. Percentages presented with correction for 10% overlap in TiO2 content between groups (see Material and Methods). §Values for today based on observed meteorite falls, not chrome spinel. *This study.

8 Table S2. Overview of variables affecting the micrometeorite flux estimates Sed. rate (cm Time window (Ma ago) (21) EC32 (grains kg-1) EC63 (grains kg-1) kyr-1) Early Paleocene (~66-61) 0.43 (12) 0.1169 0.0142

Late Cretaceous (~92-91) 1.00 (13) 0.1144 0.0053 Late Cretaceous (~94-92) 1.00 (13) 0.1157 0.0208 Early Cretaceous (~117-103) 0.34 (14) 0.3149 0.0145

Early Cretaceous (~145-133) 2.50 (15) 0.0478 0.0012 Middle Jurassic (~166-164) *0.01 (6) n/a 0.6636 Middle Jurassic (~168-166) 0.30 (5) 0.6226 0.0722 Late Devonian (~374-372) 0.35 (16) n/a 0.0512

Late Silurian (~426-424) 0.40 (17) 0.4798 0.0311 Middle Ordovician (~463-462) 0.34 (18) n/a 0.4510 Middle Ordovician (~466-465) 0.25 (17) >68.6274 4.6471 Middle Ordovician (~467-466) #0.07 (22, 23) 0.6632 0.0912

Middle Ordovician (~467-466) 0.34 (20) 0.2882 0.0190 Late Cambrian (~500-499) 0.16 (24) 0.7327 0.1202 Late Cambrian (~503-502) 0.16 (24) 0.4135 0.0577

EC32 = EC grains 32-63 µm large. EC63 = EC grains 63-355 µm large. *Based on a representation of our sample of 2.5-5.5 Ma (see Fig. S4 and SI Supplementary Text). #Based on a comparison of the thickness of the Megistaspis polyphemus Trilobite Zone in the Hällekis and Lynna sections.

Dataset S1 (separate file). Element analyses of chrome-spinel grains from the Cambrian (Sweden), the Jurassic (Italy and Spain) and Cretaceous (Italy) periods.

S1 References

1. A. Thickpenny, The sedimentology of the Swedish Alum Shales. Geol. Soc. Lond. Spec. Pub. 15, 511-525 (1984).

2. A. Anderson, B. Dahlman, D. G. Gee, S. Snäll, The Scandinavian Alum Shales. Sveriges Geol. Unders. 56, 1-50 (1985).

3. B. Buchardt, A. T. Nielsen, N. H. Schovsbo, Alun skiferen i Skandinavien. Geologisk Tidskrift 3, 1-30 (1997).

4. T.R. Weidner, P. Ahlberg, N. Axheimer, E.N.K. Clarkson, The middle Cambrian Ptychagnostus punctuosus and Goniagnostus nathorsti zones in Västergötland, Sweden. Bull. Geol. Soc. Denmark 50, 39-45 (2004).

5. L. Martire, Stratigraphy, facies, and synsedimentary tectonics in the Jurassic Rosso Ammonitico Veronese (Altopiano de Asiago, NE Italy). Facies 35, 209-236 (1996).

6. M. Reolid, I. Abad, The Middle-Upper Jurassic unconformity in the South Iberian Palaeomargin (Western Tethys): a history of carbonate platform fragmentation, emersion and subsequent drowning. Jour. Iber. Geol. 45, 87-110 (2019).

7. J. H. Schön, “Density”. in Handbook of Petroleum Exploration and Production, J. H. Schön, Ed. (Elsevier, Oxford 2011) Vol 8, chap. 4.

8. A. Cronholm, B. Schmitz, Extraterrestrial chromite distribution across the mid-Ordovician Puxi River section, central China: evidence for a global major spike in flux of L-chondritic matter. Icarus 208, 36-48 (2010).

9. T. D. Swindle, D. A. Kring, J. R. Weirich, 40Ar/39Ar ages of impacts involving ordinary chondrite meteorites. Geol. Soc. Lond. Spec. Pub. 378, 333–347 (2013).

10. B. Schmitz, Extraterrestrial spinels and the astronomical perspective on Earth’s geological record and evolution of life. Chem. Erde 73, 117–145 (2013).

11. Meteoritical Bulletin Database: https://www.lpi.usra.edu/meteor/metbull.php. (Accessed May 19, 2020).

12. S. Boschi, B. Schmitz, E. Martin, F. Terfelt, The micrometeorite flux to Earth during the earliest Paleogene reconstructed in the Bottaccione section (Umbrian Apennines) Italy. Meteorit. Planet. Sci. 55, 1615–1628 (2020).

13. E. Martin, B. Schmitz, A. Montanari, A record of the micrometeorite flux during an enigmatic extraterrestrial 3He anomaly in the Turonian (Late Cretaceous). Geol. Soc. Am. Spec. Pap. 542, 303– 318 (2019).

14. Pangaea Data Archiving PDI-24476. https://doi.pangaea.de/10.1594/PANGAEA.920972. (Accessed August 25, 2020).

15. B. Schmitz, P. R. Heck, W. Alvarez, N. T. Kita, S. S. Rout, A. Cronholm, C. Defouilloy, E. Martin, J. Smit, F. Terfelt, The meteorite flux to Earth in the Early Cretaceous as reconstructed from sediment-dispersed extraterrestrial spinels. Geology 45, 807–810 (2017).

10 16. B. Schmitz, R. Feist, M. M. M. Meier, E. Martin, P. R. Heck, D. Lenaz, D. Topa, H. Busemann, C. Maden, A. A. Plant, F. Terfelt, The micrometeorite flux to Earth during the Frasnian–Famennian transition reconstructed in the Coumiac GSSP section, France. Earth Planet. Sci. Lett. 522, 234–243 (2019).

17. E. Martin, B. Schmitz, H.-P Schönlaub, From the mid-Ordovician into the Late Silurian: changes in the meteorite flux after the L-chondrite parent breakup. Meteorit. Planet. Sci. 53, 2541–2557 (2018).

18. C. Alwmark, B. Schmitz, The origin of the Brunflo fossil meteorite and extraterrestrial chromite in mid-Ordovician limestone from the Gärde quarry (Jämtland, central Sweden). Meteorit. Planet. Sci. 44, 95–106 (2009).

19. P. R. Heck, B. Schmitz, S.S. Rout, T. Tenner, K. Villalon, A. Cronholm, F. Terfelt, N.T. Kita, A search for H-chondritic chromite grains in sediments that formed immediately after the breakup of the L-chondrite parent body 470 Ma ago. Geochim. Cosmochim. Acta 177, 120–129 (2016).

20. B. Schmitz, K. A. Farley, S. Goderis, P. R. Heck, S. M. Bergström, S. Boschi, P. Claeys, V. Debaille, A. Dronov, M. van Ginneken, D. A. T. Harper, F. Iqbal, J. Friberg, S. Liao, E. Martin, M. M. M. Meier, B. Peucker-Ehrenbrink, B. Soens, R. Wieler, F. Terfelt, An extraterrestrial trigger for the mid-Ordovician ice age: Dust from the breakup of the L-chondrite parent body. Sci. Adv. 5, eaax4184 (2019).

21. F. M. Gradstein, J. G. Ogg, M. D. Schmitz, G. M. Ogg, Eds., The Geologic Time Scale 2012. (Elsevier BV, 2012).

22. A. Lindskog, M.E. Eriksson, S. M. Bergström, S. A. Young, Lower–Middle Ordovician carbon and oxygen isotope chemostratigraphy at Hällekis, Sweden: implications for regional to global correlation and palaeoenvironmental development. Lethaia 52, 204-219 (2019).

23. T. Hansen, A.T. Nielsen, Upper Arenig trilobite biostratigraphy and sea-level changes at Lynna River near Volkhov, Russia. Bull. Geol. Soc. Denmark 50, 105-114 (2003).

24. T. W. Dahl, M.-L. Siggaard-Andersen, N. H. Schovsbo, D. O. Persson, S. Husted, I. W. Hougård, A. J. Dickson, K. Kjær, A. T. Nielsen, Brief oxygenation events in locally anoxic oceans during the Cambrian solves the animal breathing paradox. Sci. Rep. 9, 1-8 (2019).