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Home , Aalenian, Alsatites, Bajocian, Bathonian, Callovian, Cardioceras

Sea-Level Variations: A Reappraisal

Bilal U. Haq, Smithsonian Institution, Washington, D.C., 20013; and Institut des Sciences de la Terre, Sorbonne Universités, UPMC, 75252, , [email protected]

ABSTRACT cyclicity, in the absence of major sheets Jurassic. also paralleled these An accurate of the in the Jurassic, remains enigmatic. trends. Faunal and isotopic data imply rela- timing and magnitude of global sea-level tively warm climates for most of the trends and their short-term variations is an INTRODUCTION Jurassic, with some exceptions, lacking indispensable tool in high-resolution cor- A record of sea-level variations of the credible evidence for widespread glacia- relations, exploration, and paleoenviron- past inferred from the of con- tions in much of this period. However, the mental and geodynamic models. This tinental margins and interior basins (where relative warmth of the through paper is a reappraisal of the Jurassic sea- the movements of the shoreline can be best interval seems to have been inter- level history in view of recent updates in documented) is a key predictive tool in rupted by a cooler late time scales and a large body of new chro- . These data can through early Toarcian (Hinnov and Park, nostratigraphic data accrued since 1998, provide insights into several pre-drill 1999; Dera et al., 2009; Suan et al., 2010; when the last such synthesis was pre- assessment criteria, including the migra- Korte and Hesselbo, 2011; Korte et al., sented. A review of the Jurassic sea-level tion of reservoir in response to rises 2015). Korte and Hesselbo (2011) believe history has also been keenly awaited by and falls of , the frequency and that the may have fluctuated explorationists given that the Jurassic con- duration of subaerial exposure during low- between greenhouse and icehouse condi- tinues to be a major exploration target for stands, and the generation and preservation tions. There may also have been some the industry. As in previous eustatic mod- of source rocks during transgressions and cooler intervals in the , , els of this period, the updated Jurassic sea- highstands. The broad trends in Jurassic , and early (Rogov level curve remains largely Eurocentric sea-level variations have been known for and Zakharov, 2010), as well as a cold spell due to the limitations imposed by biostrati- some time (Vail et al., 1977; Hallam, 1978, near the Middle– transition graphic correlation criteria (provinciality 2001; Haq et al., 1987, 1988; Hardenbol et (in the late Callovian) (Dromart et al., of ammonite and zones), al., 1998; Haq and Al-Qahtani, 2005), but 2003). Most of the Late Jurassic is inter- though it can now be extended to some recent updates of time scales and the preted to have been relatively warmer and parts of the Tethys toward the east. The accrual of new stratigraphic data from the equable, experiencing peak warmth in the updated long-term curve indicates that period dictate a reappraisal of Jurassic (Frakes et al., 1992; there was a general rise of sea level eustatic history, especially at the third-order Zakharov et al., 2006; Brigaud et al., through the Jurassic that began close to a (shorter-term) time scales. A reappraisal 2008). Although actual global tempera- level similar to or below the present-day of the long- and short-term trends of tures and atmospheric or oceanic latitudi- mean sea level (pdmsl) in the early the base level would also be useful for nal thermal gradients of the Jurassic are Jurassic, culminating in the peak high in academic research because such informa- only conjectured, modeling indicates that the late Kimmeridgian–early tion can be the basis of stratigraphic, pCO2 levels may have been a minimum of interval, before stabilizing in the earliest pale­oenvironmental, and geodynamic four times the present-day levels (see, e.g., at ~110 m above pdmsl. Within models. In this communication, a brief Sellwood and Valdes, 2008). The long- this long-term trend are relative second- summary of the updated version of the term sea level and climatic trends also order highs in the Toarcian and Aalenian, Jurassic sea-level history is presented so show an apparent correspondence. and at Bathonian-Callovian and that it can be expediently made available to Kimmeridgian- boundaries. the research community. JURASSIC TIME SCALE Superimposed are 64 third- and fourth- The Jurassic period is currently esti- Jurassic time scales have been in a sig- order fluctuations of which 15 are consid- mated to have lasted some 55.6 m.y. nificant state of flux since the last third- ered major with base-level falls of more (201.3–145.7 Ma) (Ogg et al., 2016). The order sea-level curve for this period was than 75 m, although precise amplitudes of period saw relatively low sea levels in the published by Haq et al. (1988) or the later drawdowns are often difficult to establish. Early Jurassic, with the exception of the update by Hardenbol et al. (1998). Higher resolution fourth-order cyclicity early Toarcian, which witnessed a relative Considerable advancements have been (~410 k.y.) is also observable in many high, a variable overall lowstand in the made to better delimit the boundaries Jurassic sections whenever sedimentation , and a gradual rise there­ of the Jurassic, and the most recent effort rates were high. Causes for the third-order after that lasted through much of the Late to update this time scale was presented by

GSA Today, no. 1, doi: 10.1130/GSATG359A.1. Copyright 2017, The Geological Society of America. CC-BY-NC. Ogg and Hinnov (2012) and Ogg et al. , nannoplankton, and calpi- of the seafloor of Jurassic has since (2016). The last version of the Jurassic time onellids). In that Meso- synthesis been subducted. scale is partially based on constraints from (Haq et al., 1988; Hardenbol et al., 1998), a The documentation of the shorter-term best fits of numerical radiometric ages, special attempt was made to study all sea-level changes (third-order events) are, partially on cyclostratigraphy in strata of available stage (or neo-strato- of course, based on sequence-strati- various stages and and other isoto- type) sections (including those from the graphic information from some relatively pic data. was helpful Jurassic) that form the basis (or a global longer duration sections, but in most loca- only in the Bajocian through Tithonian standard) for biochronostratigraphy. For tions this information is pieced together interval (with a hiatus at Callovian- the , most of these sections hap- from several sections within the Jurassic. Oxfordian transition) where the low-ampli- pen to have been chosen in NW . Data from these studies were evaluated tude seafloor magnetic anomalies (from Another reason for the Eurocentricity of (and sequence-stratigraphically reinter- Drilling Program site 801 on the the Jurassic sea-level curve was the limita- preted, as needed) before inclusion in the older part of eastern ) could be tions posed by the provinciality of the current synthesis. The Jurassic paleonto- tied to magnetostratigraphy. The attempts ammonite zones that do not permit precise logical cross-correlations (i.e., zonal to astronomically fine-tune discrete inter- correlations for a truly globally based schemes based on different groups vals of the Jurassic (see, e.g., Strasser, chronology of eustatic events. These cor- and in different regions; Hardenbol et al., 2007, and a summary by Huang in Ogg relations become somewhat easier in the 1998) proved to be invaluable in aiding and Hinnov, 2012) may help with duration latest Jurassic (Tithonian) where one can correlations in some cases. The sequence- of some zonal intervals, but such piece- draw on multiple correlative tools, but for stratigraphic interpretation criteria are meal efforts do not alleviate the precision much of the Jurassic the correlation limita- well established and do not need repeti- issues of all of the stage boundaries that tions persist. In the current synthesis, all tion; however, in addition to these, other are exacerbated by the lack of reproducible available additional studies in Jurassic lithological and paleontological criteria radiometric control for much of the Middle stratigraphic sections (from 1988 through (originally listed in Haq and Schutter, and Late Jurassic. This implies that, in 2017) with good biostratigraphic data 2008; Haq, 2014) can also aid in the iden- general, the time scale of the Jurassic and were reevaluated. As a result, the correla- tification of tracts, depositional precision of the ages of many biostrati- tion net has now been widened somewhat surfaces, and sequence boundaries in out- graphic zonal boundaries still remain less to include other areas to the east in the crop and well-log sections. These include than well constrained. As Ogg and Hinnov Tethyan realm and to the Southern forced regressive facies, condensed sec- (2012) state, the Jurassic scale “should be Hemisphere; i.e., ’s Neuquén tion deposits, transgressive , evapo- considered a work in progress” and Basin, where a nearly complete Jurassic rites, carbonate megabreccias, exposure- although new constraints have refined the record is preserved (e.g., Legarreta and related deposits (i.e., incised valley fills, overall numerical chronology, “several Uliana, 1996). The heavy dependence on autochthonous coals, eolian , intervals lack adequate constraints.” Any ammonite zones for correlation means that and karst in carbonates), as well as later- future modifications of the time scale will there is a built-in uncertainty in the ages of ite/bauxite deposits. General trends in obviously necessitate the recalibration of the sequence boundaries. While the oxygen-isotopic data, in as much as they the sea-level chronology. sequence boundaries are placed according reflect broad climatic trends, can also to their relative stratigraphic position lend greater confidence to the longer-term REVISION OF THE JURASSIC within an ammonite zone (e.g., at the base, eustatic trends, and when the shorter-term SEA-LEVEL CURVE middle, top, or at the zonal boundary), isotopic excursions are distinctive, they The main correlative tool in the Jurassic theoretically the error bar could extend to can aid in the positioning of the timing of marine strata is ammonite , the entire duration of the zone or subzone the sequence boundaries within a long- occasionally assisted by other fossil in question. duration biostratigraphic zone (see Haq, groups, such as , , The long-term sea-level trends are simi- 2014, for further discussion). In this syn- calcareous nannofossils, and lar to those shown in Haq et al. (1987, 1988) thesis, d18O isotopic data from Jurassic (the last only in the Late Jurassic). In the and Hardenbol et al. (1998). The original collected from the European earlier Meso-Cenozoic sequence chrono­ long-term curve for the Jurassic was based sections (from the through stratigraphy of third-order sea-level on continental flooding data, but unlike Tithonian interval; see Martinez and changes (Haq et al., 1988, and later by the Cretaceous (see Haq, 2014), knowledge Dera, 2015) were plotted against the Hardenbol et al., 1998), the Jurassic of the oceanic crustal production rates for sea-level curve (and smoothed by Robust sequence chronostratigraphy was based on the Jurassic (i.e., variations in the mean Lowess Regression) for comparison sections in northern and central Europe age of the oceanic lithosphere, variations (see GSA Data Repository Fig. S11). The (northern and southern coasts of , in the production rates at mid-ocean general trends in these data (which repre- west-central France, southern , ridges, duration of the emplacement of sent broad climatic variations) show an and ) and their ammonite and , and large igneous provinces on apparent similarity to the long-term sea- microfossil content (mostly dinoflagellates, the seafloor) is fragmentary because most level curve, even though the ice-volume

1GSA Data Repository Item 2017387, documentation of depositional sequences comprising the new Jurassic sea-level curve, is online at www.geosociety.org/ datarepository/2018. component in the oxygen-isotopic signal come from Argentina (Mitchum and (though still a part of the western Tethys) is considered negligible in the Jurassic. Uliana, 1985; Legarreta and Uliana, 1996, follow those suggested by Hardenbol et al. An examination of the available Jurassic of the Neuquén Basin). A number (1998) and later by Ogg and Hinnov (2012). sequence-stratigraphic reports of the of other studies of the Jurassic that were Calcareous nannofossil zones of the Jurassic (up to 2017) revealed that many undertaken at the broader (second-order) Jurassic, also included, are mostly of long sections around the world cannot be cor- scales were not considered relevant for a duration and of limited correlative utility related with precision with the European third-order scale synthesis, but they do in this period. However, sometimes they stage stratotypes due to the provincial sometimes provide additional constraints do provide additional criteria for nature of ammonites, though other fossil for the long-term trends. As our ability to correlations. groups can be helpful for cross-correla- more precisely correlate sequences The two columns on the right in Figures tions. The earlier syntheses presented by improves in the future (through ancillary 1 and 2 show sea-level events (mostly Haq et al. (1988) and Hardenbol et al. fossil and other multiple, overlap- third-order and some consistent fourth- (1998) still form the basis of the current ping, correlative criteria, such as che- order sequence boundaries) and sea-level synthesis. Additional information on third- mostratigraphic methods), these deposi- curves (long-term and short-term) for the order sequences that form a part of this tional cycles may be extended to other Jurassic. When sequence boundaries are reappraisal comes from Britain and France parts of the globe where the marine correlatable in several basins they are con- (Wignall, 1991, from Kimmeridgian of Jurassic record is well preserved, such as sidered widespread (though global validity and France; Partington et al., 1993, New Zealand. cannot be verified due to the Eurocentric Kimmeridgian to Ryazanian of ; nature of most of the data). The criteria for Herbin et al., 1995, Kimmeridgian and RESULTS the long-term curves (shown in the last Tithonian of Dorset and in the column on the right) have been discussed The cycle chart resulting from the reap- UK and Boulonnais Basin in France; earlier in this paper, and the shorter-term praisal of global stratigraphic data of the Taylor et al., 2001, Late Jurassic of Wessex- sea-level curve that is derived from the Jurassic is presented as two figures (Fig. 1 ; Williams et al., 2001, sequence-stratigraphic data to its left. The for the Early Jurassic and Fig. 2 for the Kimmeridgian and Tithonian of Wessex amplitudes of third-order sea-level changes Middle and Late Jurassic). The figures Basin; Hesselbo, 2008, from the Jurassic (rise and falls in meters) shown here are represent the established biochronostratig- onshore sections of Britain); Poland averaged from stratigraphic estimates in raphy of the Jurassic, plotted against the (Pienkowski, 2004, Early Jurassic of Polish several basins and should be considered results of the current synthesis of the Basins); (Surlyk, 1990, Jurassic approximate (see discussion in Haq, 2014). sequence cycles, their revised ages (and an of East Greenland); Russia (Sahagian et They are subdivided into three magnitude updated numbering system partly adapted al., 1996, mid- to Late Jurassic of Russian categories of sea-level falls: major (>75 m), Platform; Pinous et al., 1999, Callovian to from Hardenbol et al., 1998). A sea-level medium (25–75 m), and minor (<25 m). Oxfordian of western Siberia); Portugal curve based on the onlap record is the final Most sea-level events fall within the (Leinfelder, 1993, Kimmeridgian of product of the synthesis. The biochro- medium category. ); Denmark (Johannessen nostratigraphic parts of the figures show The long-term sea-level envelope (indi- et al., 1996, and Johannessen, 2003, Late the latest (GTS 2016 of Ogg et al., 2016) cating the maximum flooding of continen- Jurassic of North Sea and Danish Central age model from the (latest tal margins and interior basins) shows that ); and northern Switzerland (Gygi stage) through (the sea level remained close to or below pres- et al., 1998, Oxfordian-Kimmeridgian; stage). This is tied to a ent-day mean sea level (pdmsl) from the Colombié and Ramell, 2007, composite paleomagnetic reversal scale latest Triassic through the Hettangian and Kimmeridgian). Other areas of the Tethys that remains tentative below the Bajocian. early Sinemurian, rising only a few tens of include the Arabian Platform (Sharland et The seafloor magnetic anomaly record is meters above pdmsl in the late al., 2001, 2004; Haq and Al-Qahtani, 2005, fragmentary below this level because the Sinemurian-Pliensbachian, and by the late mid- to Late Jurassic; Al-Husseini and older Jurassic oceanic lithosphere has been Pliensbachian it reverted back to levels Matthews, 2006, Oxfordian–early largely subducted. Even for the Bajocian comparable to pdmsl. In the Toarcian, Kimmeridgian), and (Krishna, 2005, through Tithonian interval, it is dependent there is an apparent long-term rise that mid- to Late Jurassic of Kutch Basin). For on a single site from the eastern Pacific may have peaked at ~75 m above pdmsl. In the depositional cycles identified in Tibet, (ODP site 801). The polarity scale from the the latest Toarcian, the sea levels fell again where a nearly complete Jurassic record Oxfordian to Tithonian is, nevertheless, to a few tens of meters above pdmsl, a exists (Li and Grant-Mackie, 1993), direct fairly well verified in multiple sections and trend that continued into the early correlation with the sub- third-order basins. The stages, Hettangian to Aalenian. From the late Aalenian onward, cycles of Europe and those from the west- Tithonian, currently considered standard there is a gradual sea-level rise trend, with ern Tethys could not be established due to subdivisions for the Jurassic, are tied to a few tens of meters of dip in the Bajocian differences in ammonite assemblages, but ammonite zones that, much like in the and another in the latest Callovian–earliest the authors show similarity in trends, and Cretaceous, are the most common fossil Oxfordian that culminated in the peak high even tie some of the major sequence for correlation in the Jurassic. The of the Jurassic in the late Kimmeridgian– boundaries with those in Europe. From the cross-correlation between zones from the early Tithonian. Near the Kimmeridgian- Southern Hemisphere the only data that relatively warm-water Tethyan regions and Tithonian boundary, the sea level may could be considered for this synthesis cooler-water boreal/sub-boreal regions have been as high as ~140 m above pdmsl. T. CALCAREOUS SEA LEVEL LONG-TERM AND AMMONITE ZONES NANNOFOSSIL STRA EVENTS SHORT-TERM ZONES STAGE (Sequence Boundaries) SEA-LEVEL-CURVES CHRON PERIOD

POLARITY TETHYAN BOREAL [Movement of Shoreline] TIME IN MA TETHYAN BOREAL (NJT) (NJ) TIME IN MA 250200 150100 50 0 m -50 MAGNE TO LANDWARD BASINWARD 170 170 W. LAEVISCULA H. DISCITES NJT9 170.3 JBj1 U. AA-R G. CONCAVUM NJT8c Long-term MID AA-N NJ8b B. BRADFORDENSIS curve M. AA-R MURCHISONAE 171.9 JAa3 AALENIAN NJT8b 172.6 JAa2 TO AA-N LEIOCERAS OPALINUM NJ8a 173.3 JAa1 MIDDL E NJT8a PLAYDELLIA AALENSIS UP. TO-N D. PSEUDORADIOSA D. LEVESQUEI 174.7 JTo10 175 P. DISPANSUM 175 175.6 JTo9 THOUARSENSE NJT7b MID 176.6 JTo8 TO-R 177.2 JTo7 HAUGIA VARIABILIS NJ7 178.1 JTo6 Short-term TOARCIAN 178.8 JTo5 curve 179.3 JTo4 HIDOCERAS BIFRONS NJT7a 180 180 180.4 JTo3

E. TO-N H. SERPENTIUM H. FALCIERUM NJT6 NJ6 182.3 JTo2

183 JTo1 TENUICOSTATUM NJT5b

PL-TO-R E. EMACIATUM P. SPINATUM NJ5b 184.3 JPl8 LT. NJT5a 185 A. ALGOVIANUM 185 PL-N NJ5a 186.3 JPl7 A. MARGARITATUS MID. PL.-R F. LAVINIANUM 187.6 JPl6 PLIENSBACHIAN NJT4b NJ4b 188.3 JPl5 E. PL.-N DAVOEI 188.6 JPl4 188.9 JPl3 URASSI C IBEX NJT4a NJ4a E. PL.-R 190 JPl2 190 EAR LY 190 J JAMESONI E. PL.-N 190.9 JPl1 NJT3b SN-PL.-N NJ3 191.8 JSi5 RARICOSTATUM

LT.SN-R OXYNOTUM 193.7 JSi4

195 LT.SN-N OBTUSUM NJ2b 195 SINEMURIAN NJT3a MID.SN-R CAENISITES TURNERI 196.1 JSi3

ARNIOCERAS SEMICOSTATUM 197.2 JSi2 E.SN-M NJ2a 198.2 JSi1 BUCKLANDI NJT2b NJT2a SCHIOTHEIMIA ANGULATA 200 JHe3 200 HET-N 200 HETTANGIAN LIASICUS NJT1 NJ1 P. P. PLANORBIS 200.8 JHe2 P. SPELAE 201.3 JHe1 201.8 TRh2 LT. RH-N C. MARSHI C. CRICKMAYI

LT. L.RH-M RHAETIAN C. HAUERI M.RH-N C. AMOENUM M.RH-M TRIASSIC C. SUESSI 204.5 TRh1 200150 10050 0 m -50 205 205 MAJOR CYCLE BOUNDARY MEDIUM OR MINOR CYCLE BOUNDARY POTENTIAL CYCLE BD. (NOT YET CONFIRMED)

Figure 1. Early Jurassic sequences and variations of sea level. Time scale after Ogg et al. (2016). cross-correlations are after Hardenbol et al. (1998). Sequence boundaries (sea-level fall events) are redesignated following a numbering scheme suggested by Hardenbol et al. (1998) and Snedden and Liu (2010); however, the letters Tr, J, and K are prefixed to each designation for convenience to make the numbers unique and not to confuse them with similar numbers in other periods. (Three events in the Toarcian [JTo5–JTo7] are included provisionally, pending documentation of more wide- spread occurrence.)

In the late Tithonian, the sea level is seen based on available data, which are not several basins and are thus considered to fall somewhat (from the peak high to always definitive. widespread. These third-order events show ~100 m above pdmsl at the Tithonian- As mentioned, the short-term sea-level variation in both the duration and magni- Berriasian boundary) before stabilizing in curve is largely a record of the third-order tude of sea-level falls. The timing of the the earliest Cretaceous at ~110 m above events (modeled as temporary removal or sea-level falls is accurate within a biozone pdmsl. It needs to be underscored that storage of water causing sea-level falls) (or subzone), but their numerical place- these amplitudes are at best guesstimates that have been documented consistently in ment is approximated from their position T. CALCAREOUS SEA LEVEL LONG-TERM AND AMMONITE ZONES NANNOFOSSIL STRA EVENTS SHORT-TERM ZONES STAGE (Sequence Boundaries) SEA-LEVEL-CURVES CHRON EPOCH PERIOD

POLARITY TETHYAN BOREAL [Movement of Shoreline] TIME IN MA TETHYAN BOREAL (NJT) (NJ) TIME IN MA 250200 150100 50 0 m -50 MAGNE TO LANDWARD BASINWARD 140 140 S. STENOMPHALUS M16 S. BOISSIERI S. ICENII 141.8 KBe3

CC2

CEOU S S. OCCITANICA BERRIASIAN M17 R. RUNCTONI

143.9 KBe2 M18 S. LAMPLUGHI B. JACOBI 144.7 KBe1

145 CRE TA DURANGITES CC1 145 S. PREPICOMPHALUS NJT17b M19 S. PRIMITIVUS NJT17a 146.2 JTi7 P. OPPRESSUS T. AUGUIFORMIS NJ18 M. MICROCANTHIUM G. KERBERUS G. OKUSENSIS NJT16b 147 JTi6 M20 G. GLAUCOLITHUS P. PONTI/B. PERONI P. ALBANI 147.9 JTi5 V. FITTONI NJT16a P. ROTUNDA NJ17b 148.7 JTi4 S. FALLAUXI TITHONIAN NJT15b M21 P. PALLASOIDES 149.3 JTi3 P. PECTINATUS 150 S. SEMIFORME NJT15a 150 P. HUDLESTONI 150.4 JTi2 M22 S. DARWINI P. WHEATLEYENSIS P. SCITULUS 151.5 JTi1 H. HYBONOTUM P. ELEGANS NJ16b M22A A. AUTISSIODORENSIS NJ16a 152.7 JKi7 H. BECKERI M23 A. EUDOXUS

A. EUDOXUS NJT14 153.8 JKi6 TE M24 A. ACANTHIUM A. MUTABILIS

154.5 JKi5 APPROXIMATE PRESENT-DAY SEA LEVEL C. DIVISUM 155 KIMMERIDGIAN M24A 155 M24B A. HYPSELOCYCLUM R. CYMODOCE NJ15b 155.3 JKi4 155.7 JKi3 M25 S. Short-term 156.1 JKi2 LA MIXED M25A I. PLANULA curve POLARITY P. BAYLEI M26 156.8 JKi1 157.3 JOx8 LT. E. BIMAMMATUM OX-N 157.7 JOx7 R. PSEUDOCORDATA

LT. 158.8 JOx6 OX-R P. BIFURCATUS NJT13b P. CAUTISNIGRAE NJ15a G. TRANSVERSARIUM P. PUMILUS 159.9 JOx5 160 HIGHLY MID 160 OXFORDIAN PLICATILIS 160.4 JOx4 VARIABLE OX-M POLARITY 160.8 JOx3 161 JOx2 CAR-N CORDATUM Long-term 161.8 JOx1 curve E. OX-M MARIAE NJT13a NJ14

E. OX-N 163.1 JCa6 QUENSTEDTOCERAS LAMBERTI URASSI C P. ATHLETA P. ATHLETA 164 JCa5 E. CORONATUM NJ13 E. CORONATUM R. ANCEPS K. JASON 164.5 JCa4 CALLOVIAN S. CALLOVIENSE J NJT12 165 M. GRACILIS NJ12b 165.1 JCa3 165 P. KOENIGI 165.4 JCa2 165.8 JCa1 B. BULLATUS M. HERVEYI NJ12a C. DISCUS H. RET C. DISCUS O. ORBIS H. RETROCOSTATUMC. BREMEN P. HODSONI M. MORRISIT. SUBCONTRACTUS 166.7 JBt3 P. PROGRACILIS NJT11 167.2 JBt2 BATHONIAN P. AURIGERUS NJ11 Z. ZIGZAG Z. ZIGZAG 168 JBt1 P. PARKINSONI P. PARKINSONI HIGHLY G. GARANTHIANA NJT10b 168.9 JBj4 BAJ. 169.1 JBj3 VARIABLE S. NIORTENSE NJ10 BAJOCIAN M JBj2 POLARITY S. HUMPHRRIESIANUMS. PROPINQUANS NJT10a 169.5 170 W. LAEVISCULA H. DISCITES NJ9 170 NJT9 170.3 JBj1 U. AA-R G. CONCAVUM

MIDDLE NJT8c MID AA-N B. BRADFORDENSIS NJ8b

M. AA-R LUDWIGIA MURCHISONAE 171.9 JAa3 AALENIAN NJT8b 172.6 JAa2 TO AA-N LEIOCERAS OPALINUM NJ8a 173.3 JAa1 NJT8a PLAYDELLIA AALENSIS TOARCIAN UP. TO-N D. PSEUDORADIOSA D. LEVESQUEI 174.7 JTo10 175 P. DISPANSUM NJT7b NJ7 175 250200 150100 50 0 m MAJOR CYCLE BOUNDARY -50 MEDIUM OR MINOR CYCLE BOUNDARY POTENTIAL CYCLE BD. (NOT YET CONFIRMED)

Figure 2. Middle–Late Jurassic sequences and variations of the sea level. (See Fig. 1 caption for details.)

in the outcrop sections (when sedimenta- sections (see discussion in Haq, 2014). falls are considered as major, with draw- tion rates can be calculated), and some- Fifty-six third- and eight fourth-order con- down of more than 75 m (JSi4 in times when oxygen-isotopic data are avail- sistently occurring events have been iden- Sinemurian; JPl2 and JPl8 in Pliensbachian; able that show distinct excursions from the tified in the Jurassic of the sub-boreal and JAa2, JAa3 in Aalenian; JBj1 at the base of overall trends (see the GSA Data Repository Tethyan regions, of which 25 are additional Bajocian; JOx1, JOx5, JOx6, JOx7 in [see footnote 1]). The magnitude (ampli- to the older synthesis (Haq et al., 1988). Oxfordian; JKi7 in Kimmeridgian; and tude) of sea-level falls as shown on the Three events in the Toarcian (JTo5–JTo7) JTi3, JTi4, JTi5 in Tithonian). All other curves is, however, more difficult to esti- are included here tentatively, pending events are within the medium or minor mate and has to be averaged from several wider confirmation. Fourteen sea-level range. The amplitude of sea-level falls is estimated to range from as little as <25 m and its occurrence in the Jurassic as well Frakes, L.A., Francis, J.E., and Syktus, J.I., 1992, for minor falls, to as much as ~150 m for as other periods supports the conclusion modes of the : The history that the 410-k.y. periodicity may be consid- of the ’s climate over the past 600 million major falls. The average duration of the : Cambridge, Cambridge University Press, third-order events is just over a million ered as a basic element of most sequences, 274 p., https://doi.org/10.1017/CBO9780511- years, while fourth-order events average at controlled largely by the long-term cli- 628948. ~410 k.y. Much like the Cretaceous (see matic trends. Gurnis, M., 1993, Phanerozoic marine inundation Haq, 2014), the fourth-order cyclicity also of driven by dynamic topography ACKNOWLEDGMENTS above subducting slabs: Nature, v. 364, p. 589– seems to be a common feature in the 593, https://doi.org/10.1038/364589a0. Jurassic and is observable locally in sec- This paper is dedicated to the memory of a Gygi, R.A., Coe, A.L., and Vail, P.R., 1998, tions with relatively high sedimentation fellow paleoceanographer and friend, Wolfgang Sequence stratigraphy of the Oxfordian and Berger, a scientist extraordinaire, who generously rates. This higher-order cyclicity is consid- Kimmeridgian stages (Late Jurassic) in northern shared his insights with all his colleagues. The Switzerland, in De Graciansky, P.-C., Hardenbol, ered to represent the long-period orbital author extends his thanks to Mathieu Martinez J., Jacquin, T., and Vail, P.R. eds., Mesozoic and eccentricity control on depositional cycles. and Guillaume Dera for providing the stable iso- Cenozoic Sequence Stratigraphy of European topic data on European belemnites from the Basins: Tulsa, Oklahoma, SEPM Special DISCUSSION AND CONCLUSIONS Jurassic. Special thanks are due to James Ogg, Publication 60, p. 3–29. and two anonymous reviewers, for the detailed Hallam, A., 1978, Eustatic cycles in the Jurassic: The causes for third-order cyclicity in review and many suggestions that improved this Palaeogeography, Palaeoclimatology, Palaeo­ the Jurassic, in a period where there is little paper. Thanks are also due to Alexandre Lethiers ecology, v. 23, p. 1–32, https://doi.org/10.1016/ direct evidence of major ice sheets, remain (University of Pierre and Marie Curie, Paris) for 0031-0182(78)90079-2. carefully drafting the sea-level curves through unresolved (see a discussion in Haq and Hallam, A., 2001, A review of the broad pattern of several iterations. Jurassic sea-level changes and their possible Huber, 2016). A variety of solid-Earth tec- causes in the light of current knowledge: tonic influences can affect sea-level REFERENCES CITED Palaeogeography, Palaeoclimatology, changes (see, e.g., Conrad, 2013; Haq, Al-Husseini, M., and Matthews, R.K., 2006, Palaeoecology, v. 167, no. 1–2, p. 23–37, https:// 2014). 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