aberhan (2001) -- bivalve palaeobiogeography n' the hispanic corridor-time of opening

8/18/2019 Aberhan (2001) -- Bivalve Palaeobiogeography n' the Hispanic Corridor-Time of Opening

1/21

See discussions, stats, and author profiles for this publication at:https://www.researchgate.net/publication/223375824

Bivalve palaeobiogeography and the

Hispanic Corridor: Time of opening and

effectiveness of a proto-Atlantic seaway

ARTICLE in PALAEOGEOGRAPHY PALAEOCLIMATOLOGY PALAEOECOLOGY · JANUARY 2001

Impact Factor: 2.34 · DOI: 10.1016/S0031-0182(00)00172-3

CITATIONS

63

READS

103

1 AUTHOR:

Martin Aberhan

Museum für Naturkunde - Leibniz Insti…

73 PUBLICATIONS 1,786 CITATIONS

SEE PROFILE

Available from: Martin Aberhan

Retrieved on: 01 March 2016

https://www.researchgate.net/profile/Martin_Aberhan?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_4https://www.researchgate.net/publication/223375824_Bivalve_palaeobiogeography_and_the_Hispanic_Corridor_Time_of_opening_and_effectiveness_of_a_proto-Atlantic_seaway?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_3https://www.researchgate.net/?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_1https://www.researchgate.net/profile/Martin_Aberhan?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_7https://www.researchgate.net/profile/Martin_Aberhan?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_5https://www.researchgate.net/profile/Martin_Aberhan?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_4https://www.researchgate.net/?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_1https://www.researchgate.net/publication/223375824_Bivalve_palaeobiogeography_and_the_Hispanic_Corridor_Time_of_opening_and_effectiveness_of_a_proto-Atlantic_seaway?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_3https://www.researchgate.net/publication/223375824_Bivalve_palaeobiogeography_and_the_Hispanic_Corridor_Time_of_opening_and_effectiveness_of_a_proto-Atlantic_seaway?enrichId=rgreq-03988b7e-f5e3-4721-90b0-d5357e33920f&enrichSource=Y292ZXJQYWdlOzIyMzM3NTgyNDtBUzoxMDIyMzk0MTQ3ODQwMDBAMTQwMTM4NzE4NDIyMw%3D%3D&el=1_x_2


2/21

Palaeogeography, Palaeoclimatology, Palaeoecology 165 (2001) 375–394www.elsevier.nl/ locate/ palaeo

Bivalve palaeobiogeography and the Hispanic Corridor:time of opening and eff ectiveness of a proto-Atlantic seaway

Martin Aberhan *

Museum fü r Naturkunde, Institut fü r Palä ontologie, Invalidenstr. 43, D-10115 Berlin, Germany

Received 8 December 1999; accepted for publication 19 July 2000

Abstract

The Hispanic Corridor is an embryonic seaway between the eastern Pacific and western Tethyan oceans that has

been postulated to have preceded Middle Jurassic drifting and the birth of the Atlantic Ocean by many millions of

years. In this study the distribution of pectinoid bivalve morphotypes is analysed to examine the origin of the Hispanic

Corridor and its eff ectiveness during Early Jurassic times. A comparison of pectinoid faunal similarities, based on

similarity coefficients, between various regions at opposite ends of the Corridor suggests that it opened progressively

during Early Jurassic times. However, with this approach it is difficult to exclude alternative dispersal routes, and to

determine when faunal interchange began. Analysis of the percentage of pectinoid morphotypes that were (1) present

at opposite sides of the Corridor, (2 ) simultaneously absent in the western Pacific/ eastern Tethys and ( 3) confined to

relatively low palaeolatitudes provides evidence that the Hispanic Corridor developed from an eff ective barrier in

earlier Early Jurassic (Hettangian to Sinemurian) times into a filter, allowing the passage of a few morphotypes,

during later Early Jurassic (Pliensbachian and Toarcian) times. The apparently two-way faunal exchange through the

Hispanic Corridor is consistent with the establishment of a megamonsoonal circulation for Pangaea, which may havecaused seasonally changing directions of oceanic surface currents through the Corridor. © 2001 Elsevier Science B.V.

All rights reserved.

Keywords: bivalves; Hispanic Corridor; Jurassic; palaeobiogeography; palaeoceanography

1. Introduction Atlantic Ocean a shallow marine connection was

established across rifting continental crust linking

the western end of the Tethyan Ocean with theOne of the most prominent palaeogeographic

eastern Pacific (Fig. 1). The time of formationchanges in earth history was initiated by the Earlyof this narrow passageway, called the HispanicMesozoic breakup of the supercontinent Pangaea.Corridor (Smith, 1983), and its subsequent eff ec-Although there is no direct sedimentological ortiveness for the equatorial dispersal of marinegeophysical evidence, palaeontological data sug-organisms is the subject of continuous debate andgest that prior to drifting and the birth of thewas certainly controlled by both plate-tectonic

activity and eustatic sea-level changes (e.g. Hallam,1983; Smith and Tipper, 1986; Smith et al., 1990;* Fax:+49 30 20938868.

E-mail address: [email protected] (M. Aberhan) Westermann, 1993; Stanley, 1994).

0031-0182/ 01/ $ - see front matter © 2001 Elsevier Science B.V. All rights reserved.

PII: S0031-0182( 00) 00172-3


3/21

376 M. Aberhan / Palaeogeography, Palaeoclimatology, Palaeoecology 165 (2001) 375–394

Fig. 1. Early Jurassic (Pliensbachian) palaeogeography (modified from Barron et al., 1981; Damborenea, 1987) and possible dispersalroutes for marine organisms (modified from Hallam, 1983, 1994). C1=Hispanic Corridor; C2=Viking Corridor; P1, P2=routes

around Pangaea margins; T=trans-Pacific route.

The Early Jurassic, divided into four stages 2. Early Jurassic palaeogeography and the

dispersal of marine organisms(Hettangian, Sinemurian, Pliensbachian,

Toarcian), and estimated to span about 26 million

years (Gradstein et al., 1994), is a critical time During the Early Jurassic, the supercontinent

Pangaea, surrounded by the superoceaninterval in the geological history of the Hispanic

Corridor. Based on the biogeography of the Early Panthalassa or palaeo-Pacific, was nearly symmet-

rical about the equator. About 56%

of the landJurassic bivalve genus Weyla, Damborenea andManceñido (1979) postulated the presence of a was in the northern hemisphere (Parrish, 1993;

Fig. 1). As the supercontinent began to break upshallow seaway connecting the western Tethyan

and eastern Pacific oceans as early as Pliensbachian and sea level rose during the Jurassic, several

epeiric seaways became established, separating thetimes. Biogeographical evidence from a variety of

fossil groups off ers support for this hypothesis (see areas of exposed land (e.g. Hallam, 1994). Apart

from the Hispanic Corridor, another seaway,below). In recent years, our knowledge of Early

Jurassic bivalves along the eastern palaeo-Pacific termed the Viking Corridor by Westermann

(1993), opened in Late Pliensbachian time betweenmargin has increased substantially for both western

South America (e.g. Damborenea, 1987, 1996; Greenland and Norway and connected the Arctic

and Tethys oceans.Aberhan, 1994) and western North America

(Aberhan, 1998a). In the present paper, new data Possible migration routes of shelf faunas

between the eastern Pacific and western Tethyson the distribution of a particular group of bivalves, the pectinoids, are used to: (1) analyse are indicated in Fig. 1. Apart from utilizing the

Hispanic or Viking corridors, organisms couldthe permeability of the Hispanic Corridor during

the various stages of the Early Jurassic; (2 ) investi- have migrated around the periphery of Pangaea,

either by the north or the south, or could havegate if dispersal was preferentially one-way (west–

east or east–west) or if a two-way faunal exchange crossed the palaeo-Pacific, either as long-range

dispersal of larvae or via island hopping. Finally,prevailed; and (3) consider Early Jurassic palaeo-

ceanography in the light of the results obtained it has been proposed that fossil biotas could have

been transported across the palaeo-Pacific onfrom (2).


4/21

377M. Aberhan / Palaeogeography, Palaeoclimatology, Palaeoecology 165 (2001) 375–394

various displaced terranes, which now form large adaptations and are obviously closely related.

parts of the North American Cordillera, but origi- Although a classification of taxa in morphotypesnated in more remote positions in the ancient does not reach the acuity of a species-level dataPacific. However, for the bivalve bearing Early set, a much finer taxonomic (and biogeographic)Jurassic terranes a location close to the western resolution is obtained than from genera alone. Itmargin of Pangaea is most plausible (e.g. Aberhan, avoids taxonomic biases introduced by misidenti-1998b and references cited therein). fications and contrasting species concepts of

diff erent authors, and yields a uniform taxonomic

concept in a manageable amount of time without

having to revise a whole fauna at the species level.3. Materials and methods

A definition of pectinoid morphotypes, which are

named after a characteristic representative, is pre-3.1. Early Jurassic pectinoid bivalves

sented in Appendix A.

The present analysis is based on the distribution

of bivalves of the order Pectinida. Representatives3.3. The studied areas and temporal framework

of this sessile group of organisms are fairlycommon and well preserved in the studied areasThe geographic areas selected for the study werewhere they occur in a wide range of environments.

lumped into five major geographic units. TheseTheir diversity is well documented in the literature,are: (1) northwestern Europe (Great Britain,and a uniform taxonomic concept can be applied.Sweden, Denmark, Belgium, Luxemburg,What little is known about the larval developmentGermany, Switzerland, northern France); (2) west-of Jurassic pectinoids (Palmer, 1989) and theirern Tethys (SW-France, Italy, Spain, Portugal,modern counterparts ( Waller, 1991) suggests thatMorocco, Algeria); (3 ) western South Americathey possessed planktotrophic larvae, and there-(Colombia, Peru, Chile, Argentina); (4) westernfore depended on oceanic currents for their dis-North American craton (Huayacocotla trough of persal (but see Waller, 1993 for an example of aeastern Mexico, western Nevada, northernlecithotrophic-type larval shell in a reef-adapted

California, cratonal areas of western Canada); andpectinid from the Caribbean). Recently, distribu-(5) western North American terranes (Antimoniotional patterns of pectinoid bivalves proved usefulterrane of NW-Mexico, Wrangellia, Stikinia,in constraining the Early Jurassic tectonic evolu-Quesnellia, Cadwallader terrane). The areas of thetion of western Canadian terranes (Aberhan,last category are crustal fragments that are alloch-1998b, 1999), thus testifying to their high potential

thonous relative to the autochthonous craton, butin geologically orientated palaeobiogeographic

analyses. palaeogeographic evidence suggests proximity to

the North American craton throughout the Early

Jurassic (e.g. Smith and Tipper, 1986; Aberhan,3.2. The morphotype concept1998b). Data for comparison with the western

Pacific were included where deemed necessary.Studies on Jurassic bivalve biogeography are

The data (see Appendix B and references citedusually carried out at the generic/ subgeneric level.therein) were analysed separately for four timeCompared with species-based data sets, this clearlyintervals corresponding to the four stages of results in the loss of potentially useful information.the Early Jurassic: Hettangian, Sinemurian,On the other hand, a sound taxonomic databasePliensbachian and Toarcian. Only records withat species level is not feasible in most cases, especi-illustrations entered the database, provided thatally if large data sets are involved. The morphotypethe specimens were well preserved enough to allowconcept, as applied in the present study, forms aassignment to a morphotype and the age wascompromise. A morphotype groups together

species that exhibit very similar morphological determinable at the stage level. Faunal affinities of


5/21


the various areas to each other are established by

calculating Dice (D) and Jaccard (J ) similarity

coefficients. These coefficients are defined as

D=[2C / (N 1+N

2)]×100

and

J =[C / (N 1+N

2−C )]×100

where N 1 is the number of taxa in sample 1, N

2 is

the number of taxa in sample 2, and C is the

number of taxa common to both samples.

4. Results

4.1. Comparison of faunal similarities

Dice and Jaccard similarity coefficients show

exactly the same temporal trends (e.g. Fig. 2A),

and therefore only Dice coefficients are reproduced

in Fig. 2B and C.

In order to gain an overall impression of the

faunal similarities between the eastern Pacific and

the western Tethys and adjacent epicontinental

seas of NW-Europe, data for the three eastern

Pacific areas and those for the two European/ NW-African areas were combined (Fig. 2A). The

similarity of pectinoid bivalves increases steadily

from comparatively low values in the HettangianFig. 2. Early Jurassic similarities of pectinoid bivalve morpho-and Sinemurian to intermediate values in thetypes between western Tethys, NW-Europe and various eastern

Pliensbachian and highest values in the Toarcian.Pacific regions. (A) Increasing Dice and Jaccard coefficients

If the data from the various eastern Pacific areas between eastern Pacific and Europe/ NW-Africa suggest pro-are compared with the western Tethyan Ocean gressive opening of the Hispanic Corridor. (B) Dice coefficients

between western Tethys and various eastern Pacific areas. (C)(Fig. 2B), pectinoids from the North AmericanDice coefficients between NW-Europe and various easterncraton and those from the terranes show a trendPacific areas.

of increasing similarity to the western Tethys with

time. Dice coefficients between South America and

the western Tethys are higher than those for theother two Pacific areas. Values fluctuate around a Hettangian to lower values in the Sinemurian and

Pliensbachian and reaches a peak in the Toarcian.level of 45 from Hettangian to Pliensbachian times,

and show a marked increase in the Toarcian. In a

very similar way, similarity values between both 4.2. Dispersal of selected morphotypes

the North American craton and the terranes and

those from NW-Europe (Fig. 2C) increase through As a next step we analyse how the distribution

of morphotypes can contribute to the reconstruc-time. Similarity between the South American

craton and NW-Europe decreases from the tion of the early development of the Hispanic


6/21


Corridor. In order to preclude alternative dispersal European areas, this morphotype does not provide

any clues concerning the opening of the Hispanicroutes, a taxon must fulfil three criteria, at leastCorridor. Western Pacific records of the other fourduring the early phases of its duration: (1) presencemorphotypes are of the same ages as first occur-on either end of the Hispanic Corridor; (2 ) simul-rences on opposite sides of the Hispanic Corridor:taneous absence in western Pacific regions; andOxytoma cygnipes (Hettangian of New Zealand,(3 ) confinement to relatively low palaeolatitudes.Damborenea and Manceñido, 1992); EntoliumOf the 48 morphotypes considered in this study,corneolum ( Toarcian of North-East Russia,15 meet criterion (1) (see Appendix A). In orderMilova, 1988); Entolium lunare (Sinemurian of to evaluate criterion (2), the possible presence of Japan, Hayami, 1975); and Chlamys valoniensisthese morphotypes in the North-East and Far East(Hettangian of North-East Russia, Milova, 1976;of Russia, in Japan and in New Zealand wasHettangian/ Early Sinemurian of New Zealand,explored. A survey of the relevant literature revealsDamborenea and Manceñido, 1992). Because athat seven morphotypes appear to be absent fromdispersal route other than the Hispanic Corridorwestern Pacific regions, at least throughout Earlycannot be excluded, these morphotypes are notJurassic times, and therefore meet criterion (2):considered further here.Placunopsis striatula, Pseudopecten equivalvis,

For the 10 morphotypes that fulfil criteria (1)Camptonectes auritus, Camptonectes subulatus,and (2), the known Early Jurassic palaeolatitudi-Eopecten abjectus, Eopecten velatus and Weylanal ranges are presented in Table 1. Three morpho-meeki . To these may be added, Oxytoma inequi-types (Oxytoma inequivalvis, Placunopsis striatula

valvis, Propeamussium pumilum and Chlamys texto-and Chlamys textoria) were spread over a relatively

ria. Although known from western Pacific areasbroad palaeolatitudinal range during the Early

during Early Jurassic times (see Efimova et al.,Jurassic, and may have used a variety of alternative

1968; Milova, 1976, 1985, 1988; Hayami, 1975;migration routes. The remaining seven morpho-

Sey, 1984; Sey and Polubotko in Damboreneatypes, however, seem to be confined to a belt

et al., 1992), all these records are younger thanextending from about 40° north to 45° south of

their first occurrences at opposite ends of the

Hispanic Corridor. The diff erence in age is smallest

for Propeamussium pumilum. Its first appearanceTable 1in the Pliensbachian of Europe (Johnson, 1984) isSelected morphotypes of pectinoid bivalves and their Early

followed by apparently contemporaneous occur- Jurassic palaeolatitudinal ranges. N=northern palaeolatitude;rences in the Toarcian of South America and S=southern palaeolatitude. Records from the North-East and

Far East of Russia are not considered as they are commonlyNorth-East Russia. However, as records fromfrom terranes, the Early Jurassic palaeolatitudinal positions of South America are from the Early Toarcian (e.g.which are poorly constrained. For discussion see text. Data

Hillebrandt and Schmidt-Effing, 1981; Aberhan,based on Aberhan (1994, 1998a,b), Damborenea (1996),

1994), they predate the mid-Toarcian occurrence Damborenea and Manceñido (1979), Johnson (1984),in eastern Russia (Polubotko and Repin, 1988), Trechmann (1923) and unpublished information

and consequently this morphotype is potentiallyMorphotype Palaeolatitudinal range

useful in constraining the early history of the

Hispanic Corridor. Oxytoma inequivalvis 60°N–75°SPlacunopsis striatula 70°N–42°SFrom the five morphotypes that do not meetPropeamussium pumilum 35°N–45°Scriterion (2), one (Meleagrinella substriata)Pseudopecten equivalvis 40°N–40°S

appears to have occurred first during theCamptonectes auritus 30°N–35°S

Hettangian in North-East Russia where it is repre- Camptonectes subulatus 40°N–35°SChlamys textoria 70°N–45°Ssented by the species Meleagrinella subolifexEopecten abjectus 35°N–38°SPolubotko (Efimova et al., 1968; Sey andEopecten velatus 35°N–35°SPolubotko in Damborenea et al., 1992). As this isWeyla meeki 40°N–30°S

earlier than oldest records from eastern Pacific and


7/21


the palaeoequator. Their restriction to relatively origination rates of endemics were very high from

Late Sinemurian to Late Pliensbachian timeslow palaeolatitudes, simultaneous presence in

Europe and along the eastern Pacific margin, and (Aberhan and Fürsich, 1997, 2000). However, a

generally high percentage of Andean endemicsabsence, or at least stratigraphical restriction to

younger stages, from western Pacific and eastern cannot explain the relatively low similarity of

pectinoid morphotypes in mid-Early Jurassic timesTethys suggest dispersal via the Hispanic Corridorat various times during the Early Jurassic. between South America and NW-Europe. In fact,

the percentages of pectinoid morphotypes that are

endemic to either NW-Europe or South America

are by no means significantly higher during the5. Discussion

Sinemurian and Pliensbachian than during the

Hettangian and Toarcian ( Fig. 3).5.1. Interpretation of faunal similarity patterns

This suggests that it is high Hettangian rather

than low Sinemurian and Pliensbachian similarityThe general trend of pectinoid bivalves is a

progressive increase in similarity between the west- that deviates from the normal trend. Examination

of the six Hettangian morphotypes common toern Americas and Europe during the Early Jurassic

(Fig. 2). The most marked exceptions are South America and NW-Europe reveals that onlytwo, Camptonectes subulatus and Eopecten velatus,Sinemurian and Pliensbachian similarity values

between South America and NW-Europe, which are considered as candidates for dispersal through

the Hispanic Corridor (see Section 4.2). Since theyare relatively low in comparison with the

Hettangian value (Fig. 2C). A diversity analysis are first recorded from the pre- planorbis beds

and the planorbis Zone respectively, their originsof bivalves from the Andean basins showed that

Fig. 3. Degree of endemism of pectinoid bivalve morphotypes in Early Jurassic time. Data based on Appendix B; absolute age dates

from Gradstein et al. (1994).


8/21


probably lie in the Triassic (Johnson, 1984). Their data set. By analogy, the pectinoid data presented

herein are compatible with the concept of theoccurrence in South America and Europe may

Hispanic Corridor opening progressively duringbe the result of dispersal around southernEarly Jurassic time. The major shortcomings of Gondwanaland or along a circum-Laurasian routeHallam’s approach, however, are that the latitudi-during the Late Triassic ‘hothouse’ climate system.

nal range of taxa as well as data from the westernFor these reasons, relatively high Hettangian DicePacific and eastern Tethys are not taken intocoefficients between South America and Europeanaccount. As a consequence, it is impossible toareas are unlikely to reflect migration via thedisentangle the relative importance of high versusHispanic Corridor in earliest Jurassic time.low palaeolatitude migration routes, and to deter-Applying a similar approach, Hallam (1983)mine when the interchange of organisms began.has analysed the similarity of Jurassic bivalve

genera between Europe, North America and South

America. Rising Simpson similarity coefficients5.2. Excluding alternative dispersal routesbetween Europe and the western Americas (Fig. 4)

are in good agreement with similarity curves of Whilst a similarity study with only a few regionspectinoid morphotypes (Fig. 2) . Hallam’s data

fails to test if and to what degree the Hispanicwere interpreted to indicate that some degree of Corridor was utilized for migration by organisms,isolation persisted between the Americas andanalysis of distributional patterns holds muchEurope as at first only a few organisms filteredmore promise. Because of ample data, establish-through the Hispanic Corridor, and that relativelyment of the presence/ absence of pectionoidfree intermigration was established by the Middlemorphotypes on opposite sides of the HispanicJurassic (Hallam, 1983; Smith and Tipper, 1986;Corridor and in the western Pacific was fairlySmith, 1988). These conclusions were essentiallystraightforward. Less information is available fromconfirmed in a recent analysis by Damboreneathe eastern Tethys, the pre-Toarcian bivalve record(2000), who used the same method as Hallam,of which is rather poor or lacking, and from highalthough within a temporally and spatially morepalaeolatitude areas.finely resolved framework and with an updated

Data from high northern and southern areasare considered as particularly important for evalu-

ating high latitude routes for dispersal. Although

the concept of climatic equability in the Jurassic

has been challenged recently (Crowley and North,

1991), there is no doubt that temperature gradients

from the equator to the poles were distinctly lower

compared with the present (e.g. Hallam, 1998 and

references cited therein). Still, the geographic

diff erentiation of Early Jurassic bivalves into

boreal, austral, bipolar and low latitude forms

(Damborenea, 1993, 1996; Aberhan, 1998b, Liu

et al., 1998), and the well-known Tethyan–Borealprovinciality among the ammonites (e.g. Hallam,

1994), suggest that environmental conditions

varied enough to produce latitudinally distinct

faunas. Although documented less intensely, the

absence of a pectinoid morphotype from suchFig. 4. Simpson similarity coefficients of bivalve genera between

relatively high palaeolatitude areas as the southernthe western Americas and Europe through time as calculated

Andes and New Zealand in the southern hemi-by Hallam (1983). Absolute age dates from Gradstein et al.(1994). sphere, and northwestern Canada, Arctic Canada


9/21


and East Greenland in the northern hemisphere, With respect to low palaeolatitude routes, an

alternative to the Hispanic Corridor is long-rangeis therefore regarded as adequate evidence to

render unlikely its dispersal around southern larval dispersal across the ancestral Pacific. For

Pangaean times, tropical trans-oceanic faunal dis-Gondwanaland, northern Laurasia or via the

Viking Corridor. persal was hypothesized both from east to west

(e.g. Kristan-Tollmann and Tollmann, 1982), andThe palaeolatitudinal range from 40°N to 45°S,inferred for those five morphotypes that have from west to east (e.g. the pantropical model of

Newton, 1988; see comments by Smith et al.,apparently utilized the Hispanic Corridor (see

Sections 4.2 and 5.1, Table 1), seems to be fairly 1990). For the five pectinoid morphotypes under

discussion, the apparent absence in the westernlarge to be called ‘low latitude’, but is compatible

with palaeoclimatic data. In the Early Jurassic Pacific and eastern Tethys renders a trans-Pacific

dispersal more unlikely than migration throughterrestrial realm, phytogeographic data suggest

that the transition from warm to cool-temperate the Hispanic Corridor. In addition, it is known

that open oceans act as eff ective barriers to dis-conditions in the northern hemisphere took place

at about 45° (Ziegler et al., 1993), and growth persal of many marine invertebrates, and during

Early Jurassic times the central palaeo-Pacificring studies of fossil wood indicate a broad equato-

rial zone ranging in latitude from approximately ocean was at its widest (Smith and Tipper, 1986;Smith et al., 1990).30°N to 30°S (Creber and Chaloner, 1984).

Fig. 5. Postulated origination and subsequent dispersal of five pectinoid bivalve morphotypes during Early Jurassic time. Geographic

distribution and timing of occurrences suggest that dispersal through the Hispanic Corridor occurred during Pliensbachian and

Toarcian times.


10/21


5.3. Origin of the Hispanic Corridor To put these results in perspective, literature

data on time and direction of dispersal of various

fossil groups via the Hispanic Corridor, includingThe European and eastern Pacific stratigraphic

ranges of the five morphotypes considered to have calcareous sponges, corals, bivalves, ammonites,

belemnites and brachiopods, are summarized inused the Hispanic Corridor indicate that three of

them migrated during Pliensbachian and two Table 2. These data are consistent with the resultsof the present study, and point at an initial openingduring Toarcian times (Fig. 5, Table 2). Even if

it cannot be excluded from the available data in early Pliensbachian time. Only in one case

has an earlier origin been inferred (Stanley andthat a few morphotypes migrated prior to the

Pliensbachian, there is no unequivocal support for Beauvais, 1994). Based on the distribution of

corals, these authors conclude that the Hispanicthis hypothesis. This argues for an opening of the

Corridor in the Pliensbachian, and suggests that it Corridor may have played an important role

during Sinemurian time. Their data, however,was not a viable dispersal route for pectinoid

bivalves during earliest Jurassic times. The sim- imply east–west dispersal of two coral species in

late Hettangian time and west–east dispersal of ilarity curve (Fig. 2A) is consistent with a

Pliensbachian origin of the Hispanic Corridor, but two other species later in the early Pliensbachian

(Stanley and Beauvais, 1994, fig. 7). Whilst theof course does not prove it (see discussion above).

Table 2

List of marine invertebrates bearing on the Early Jurassic origin of the Hispanic Corridor. Het=Hettangian; Plb=Pliensbachian;

Toa=Toarcian; E–W=from east to west; W–E=from west to east

Taxon Group Presumed time Direction Reference

of dispersal

Stylothalamia calcareous sponge early Plb E–W Hillebrandt, 1981

Phacelostylophyllum rugosum, corals late Het E–W Stanley and Beauvais, 1994

Actinastrea plana

Stylophyllopsis victoriae, corals early Plb W–E Stanley and Beauvais, 1994Actinastrea minima

Camptonectes auritus, bivalve morphotypes Plb E–W this study

Pseudopecten equivalvis

Eopecten abjectus, bivalve morphotypes Toa E–W this study

Propeamussium pumilum

Weyla meeki bivalve morphotype Plb W–E this study

Weyla bivalve early Plb W–E Damborenea and Manceñido, 1979, 1988;

Hallam, 1983

Lithiotis (=Plicatostylus) bivalve Plb – Loriga and Neri, 1976; Hillebrandt, 1981;

Hallam, 1983; Nauss and Smith, 1988

Opisoma bivalve mid Toa E–W Hillebrandt, 1981; Hallam, 1983;

Aberhan and Hillebrandt, 1999

Bouleiceras ammonite early Toa – Hillebrandt, 1973

Dayiceras/ Dubariceras ammonites early Plb – Smith, 1983; Smith and Tipper, 1986Frechiella ammonite mid Toa – Hillebrandt, 1973

Leukadiella, Paroniceras ammonites mid Toa – Hillebrandt and Schmidt-Effing, 1981;

Jakobs, 1995

Oregonites ammonite Plb – Smith and Tipper, 1986

hastitid ancestors of Dicoelitidae belemnites latest Plb or E–W Jeletzky, 1980

earliest Toa

Thecideaceans brachiopods late Plb E–W Manceñido and Damborenea, 1990;

Baker and Manceñido, 1997

Squamiplana (Cuersithyris) brachiopod early Plb – Manceñido and Dagys, 1992


11/21


latter event is consistent with all the other data

presented in Table 2, a late Hettangian age seems

surprisingly old. Even more extreme is the hypoth-

esis of a corridor being in existence possibly as

early as the Late Triassic, which was based on the

palaeobiogeography of brachiopods and corals(Sandy and Stanley, 1993; Stanley, 1994 and refer-

ences cited therein). Fluctuations in eustatic sea-

level and tectonic activity along the corridor areFig. 6. Percentage of pectinoid morphotypes that apparentlyregarded as the main control of its eff ectiveness.utilized the Hispanic Corridor for the first time during the fourDuring Hettangian time, Jurassic eustatic sea-levelstages of the Early Jurassic. Numbers in the diagram indicate

was at its lowest stand, and Late Triassic sea-levelthe total number of morphotypes per time interval.

was characterized by a major regression (e.g.

Hallam, 1992). This is in accord with the Late

Triassic to earliest Jurassic stratigraphic record of

the numerous rift basins along the postulated that also extend into high palaeolatitudes and

western Pacific/ eastern Tethys areas obviouslycorridor, which consists of continental sequencescomprising lacustrine and fluvial clastic rocks, could tolerate a broad range of environmental

conditions. As eurytopic taxa they are also theevaporites, coals and basalts (Olsen, 1997). The

salt deposits apparently formed in evaporitic lakes most likely to spread through a filter, in which

strong fluctuations in environmental parametersand continental playa or sabka environments fed

by non-marine waters. Marine sediments, includ- such as temperature and salinity can be expected.

Restriction to low palaeolatitude taxa excludesing salt deposits of a probably marine source, are

limited to the opposite ends of the rift in Spain, these potential travellers, and the number of those

that actually passed through the corridor may bewest of Morocco and in Mexico (Smith and

Tipper, 1986; Stanley, 1994 and references cited somewhat higher. Nevertheless, such a low percen-

tage of pectinoid morphotypes travelling along thetherein). For these reasons, the idea of a pre-

Jurassic to earliest Jurassic marine connection Corridor suggests that it acted as a filter duringPliensbachian and Toarcian times. This view isseems to be very speculative, and needs to be

tested rigorously against other models such as supported by the observation that, in contrast to

some shallow water bivalves, Early Jurassic ‘off -trans-Pacific dispersal.

shore’ genera, such as Posidonotis and Otapiria,

were unable to pass the Corridor (Damborenea,

2000, but see discussion on the distribution pattern5.4. E ff ectiveness of the Hispanic Corridor

of Posidonotis in Aberhan and Pálfy, 1996).

Studies comparable with the present one, whichReflecting its eff ectiveness a migration route

may be classified as a corridor if it allows relatively determine the percentage of a fauna that migrated

via the Hispanic Corridor, have not been carriedfree migration, or as a filter if it allows the passage

of some organisms but not others. A very eff ective out so far. But again, faunal similarities of bivalves

(Hallam, 1983; Damborenea, 2000; Figs. 2 and 4)barrier that could only be overcome by chanceevents is called a sweepstake route (Simpson, 1940; are compatible with the hypothesis of a pro-

gressively opening marine connection from EarlyMcKenna, 1973). During Pliensbachian times, 35

pectinoid morphotypes are recognised, 8% of to Middle Jurassic times. Both palaeobiogeo-

graphic and geological evidence indicate that awhich apparently passed through the Hispanic

Corridor ( Fig. 6) . In the Toarcian (28 morpho- relatively open corridor was in operation, at least

intermittently, in Middle and Late Jurassic timestypes) this number is slightly less (7%). Due to the

rigorous criteria applied to identify corridor voyag- (e.g. Hallam, 1977, 1983; Westermann, 1977, 1993;

Riccardi, 1991; Boomer and Ballent, 1996).ers, these values may be too low. Widespread taxa


12/21


Development from a filter into a corridor is paral- ammonites, transport of eggs may be more impor-

tant factors than the ecological requirements of leled by an overall rise in Hallam’s (1988) eustaticadults.sea-level curve of the Jurassic. Obviously, this

increase in sea-level was not compensated by tec-

tonic activity along the rift, and probably both5.5. A two-way migration routeprocesses have reinforced each other.

The ecological diversity of bivalves, charac- Stratigraphic age relationships provide clues toterized by various life habits and feeding modes, the direction of migrations. From the five morpho-makes this group a potential source of information types considered to have used the Hispanicon the physical conditions existing along the route. Corridor for dispersal, four originated in EuropePectinoid bivalves are an epifaunal suspension- (Fig. 5; Table 2). Only Weyla meeki occurred firstfeeding group, and individual taxa belong to the in the eastern palaeo-Pacific. This indicates thatfree-lying, byssate and cemented guilds. Whilst among pectinoids east–west migration prevailed.Eopecten abjectus shows a strong preference In contrast, for late Toarcian–Aalenian times,for condensed ferruginous oolites, the species Hallam (1983) concluded that bivalve traffic was

Propeamussium pumilum, Camptonectes auritus, largely one-way, as eastern Pacific taxa moved

eastward to occupy habitat space which had beenPseudopecten equivalvis and Weyla meeki werevacated during the Early Toarcian mass extinctionremarkably eurytopic with respect to the substrateof bivalves in Europe. Examination of Table 2,(Johnson, 1984; Aberhan, 1998b). P. pumilum washowever, shows that Early Jurassic migrationalso able to live under variable conditions of from east to west was at least as common as inoxygen tension and turbulence, and probably hadthe opposite direction. This view of a two-wayan opportunistic adaptive strategy (Johnson, 1984;migration route is corroborated by several bivalveAberhan, 1993); C. auritus could cope with highgenera (including oysters, bakevelliids andphysical stress, oxygen deficiency and various tem-trigoniids), which, according to their knownperatures (Johnson, 1984), and was also reporteddistribution through time, probably migratedfrom the upper brachyhaline salinity regime, closealong the Corridor (Damborenea, 2000). Similarly,to fully marine conditions (e.g. Fürsich, 1993);

Westermann and Riccardi (1985) did not recogniseand P. equivalvis was able to tolerate high levelsa preferred direction in the migration of Middleof water energy (Johnson, 1984). Such broadJurassic ammonites through the Corridor.environmental tolerances are additional evidence

that the Corridor was an ecological barrier that

could only be overcome by eurytopic taxa.

Considering the large amounts of evaporites that 6. Biotic dispersal through the Hispanic Corridorhave been deposited in the rifts, it seems likely and Early Jurassic palaeoceanographythat extreme salinities or strongly fluctuating salin-

ity values were limiting biotic exchange. This may On an evolutionary time scale, organisms withexplain the low percentage of pectinoids, which a holopelagic life cycle have the potential to occurare at best subordinate faunal components in virtually everywhere, provided their ecological

salinity-controlled Mesozoic environments. On requirements are met. Sessile, benthic organismsthe other hand, ammonites apparently used the such as pectinoid bivalves depend more stronglyCorridor from Pliensbachian times onwards on oceanic currents for their dispersal during the(Table 2), although they could not cope with larval stages. Given the apparently two-way faunalpalaeosalinities which deviated from normal exchange through the Hispanic Corridor, oceanicmarine values. In this respect it would be interes- circulation must have been favourable for larvalting to analyse the dispersal of other bivalve groups transport in both directions. In principal, oceanicsuch as the relatively euryhaline oysters. Anyway, circulation is driven by wind stress and by density

variations of seawater. In the following Ithe ecology of bivalve larvae and, in the case of


13/21


speculate on the possible influence of both factors northern summer. As a consequence, the southeast

on oceanic circulation through the Hispanic trade winds would have blown across the palaeo-Corridor. equator and, having been diverted to the right by

the Coriolis force, would give rise to a current

flowing from the eastern Pacific to western Tethys.6.1. Wind-driven circulation Current flow through the Corridor in opposite

directions would have happened semi-annually.Present-day equatorial current systems in the Such a reversal of the normal trade wind pattern

open oceans are a direct result of the trade winds. across the continent is in agreement with changesThese blow at about 45° to the equator and induce of surface wind vectors obtained in numericalwestward flows in the surface water (the north and model simulations of Pangaean climates (seesouth equatorial currents). An eastward flowing models of Kutzbach and Gallimore, 1989;equatorial countercurrent is driven by the hori- Chandler et al., 1992).zontal pressure gradient that is set up when west-

ward flowing surface water is blocked by a

landmass and the sea-surface slopes up to the 6.2. Density-driven circulation

west.Predicted equatorial ocean currents of the Early The density of seawater is controlled by varia-

Jurassic palaeo-Pacific are similar to those encoun- tions in temperature and salinity. The Mesozoic istered in the modern Pacific (Parrish, 1992). With generally conceived as a time interval when thethe opening of the Hispanic Corridor some temperature distribution was more even thanthroughflow of the equatorial current may have today, so that salinity becomes an important factorintroduced warm Tethyan surface water into the

in the density of seawater. It is therefore possiblePacific. However, it is unlikely that during this

that vertical circulation in the Mesozoic oceansembryonic stage of the Atlantic Ocean a circum-

was driven largely by salinity diff erences ratherglobal, westward flowing equatorial current was

than primarily by temperature as today (e.g. vanfully established.

Andel, 1994). In the case of the Hispanic Corridor,

An Early Jurassic equatorial countercurrent, it is conceivable that a thermohaline circulationflowing eastward through the Hispanic Corridor,was established similar to that between the

is not a viable hypothesis. In the case of westwardpresentday Mediterranean and Atlantic Ocean.

throughflow of the equatorial current a counter-Evaporation in the Mediterranean Sea in summer

current would not have existed at all. In contrast,exceeds the influx of freshwater, and high-salinitywith a barrier in place across western Tethys, thesurface water is formed. When this surface waterequatorial countercurrent may have been strongcools in winter it sinks, and flows out at depth(Parrish, 1992). However, at the western end of into the Atlantic Ocean, and relatively low-the Hispanic Corridor its driving force, the west– salinity water flows into the Mediterranean ateast diff erence in sea level across the palaeo-Pacific,the surface.was no longer eff ective.

While the western end of the Hispanic CorridorBecause of its size and the distribution of land

was close to the equator, its eastern end wasin both hemispheres, a strong monsoonal circula-located in the subtropics at about 25°N during thetion should have existed for Pangaea (e.g.Pliensbachian ( Fig. 1). Considering this diff erenceKutzbach and Gallimore, 1989; Parrish, 1992,in palaeolatitudes and the extension of the1993). During the northern winter, northeast tradeCorridor from one margin of a supercontinent towinds would have generated a westward flowingthe other, it can be expected that palaeoclimatolog-current through the Hispanic Corridor. In analogyical parameters diff ered at opposite ends of theto the present-day summer monsoonal circulationseaway. Information on palaeoclimate and onin Asia, the intertropical convergence zone would

have shifted considerably northward during the the kind of water masses can be obtained from


14/21


geological data and from conceptual and numerical currents flowing through the Hispanic Corridor,

and deserves further testing and modelling. Theclimate models. During the Late Triassic and earli-

est Jurassic, salt deposits in the eastern and central densities of water masses in the equatorial eastern

Pacific and subtropical western Tethys, and theirpart of the rift suggest extreme arid conditions,

which contrast with synchronous lake, playa and seasonal variability, are insufficiently known at

present, and it is difficult to evaluate how theycoal swamp deposits in basins in the western partof the rift complex (Hay et al., 1982). The aff ected oceanic currents within the Corridor.

From the available evidence it seems possible thatonly Lower Jurassic marine sediments known at

the western end of the Corridor are in the a density-driven current reinforced a wind-driven,

eastward flowing current that was in operationHuayacocotla trough of eastern Mexico, which

Schmidt-Effing (1980) has interpreted as an aulao- during the northern summer.

cogen associated with the opening of the Gulf of

Mexico. The marine sedimentary fill consists of

shales, siltstones and sandstones of Sinemurian

age, which suggest relatively humid conditions. In

contrast, the Early Jurassic carbonate platform 7. Conclusions

deposits of western Tethys and the abundant EarlyJurassic evaporites in northern Africa and north- Palaeobiogeographic patterns of pectinoid

bivalve morphotypes provide further evidence thateastern North America apparently formed under

more arid conditions. the Hispanic Corridor was in existence during

Early Jurassic times. In order to determine its timeFor Pliensbachian time, conceptual models of

rainfall patterns predict relatively high rainfall in of formation and subsequent eff ectiveness, the

current method of calculating similarity coefficientsthe equatorial eastern Pacific and moderately low

rainfall in the western Tethys (Parrish et al., 1982; alone seems to be insufficient. The presence of

common taxa in a few areas at opposite sides of Parrish, 1992). Numerical modelling of Pangaean

climate during the Early Jurassic yielded very high the Corridor does not, in itself, imply a proto-

Atlantic marine connection because several alter-evaporation rates in western Tethys, particularly

during the northern winter (Chandler et al., 1992). native dispersal routes cannot be ruled out. Amore rigorous approach is to identify the percen-In this model, however, the annually averaged

precipitation minus evaporation values are nega- tage of taxa per time interval that were (1) present

at opposite sides of the Corridor, (2 ) simulta-tive at both ends of the Corridor, and it is difficult

to assess their seasonal variability. Nevertheless, it neously absent in the western Pacific/ eastern

Tethys and (3) confined to relatively low palaeolat-is conceivable that, during the Early Jurassic,

supersaline surface water formed by evaporation itudes. The results suggest that during Hettangian

and Sinemurian times the future site of thein the western Tethys and sank into deep basins,

thereby causing a flow of eastern Pacific surface Hispanic Corridor most likely was an eff ective

barrier to the spread of marine organisms. Thewater through the Hispanic Corridor into western

Tethys. The Corridor was relatively shallow and Hispanic Corridor first opened in the

Pliensbachian and acted as a filter until Toarcianthe floor of the rift system probably had a marked

relief. Because vertical barriers could hinder the times, providing a restricted level of faunalexchange between the eastern Pacific and westernmovement of saline bottom currents, it is unclear

to what extent a bottom return flow of relatively Tethys oceans. Apparently, development into a

marine corridor was not before the Middlehigh salinity carried water from the western Tethys

back to the eastern Pacific. Jurassic. Bidirectional faunal exchange through

the Corridor is in agreement with the establishmentIn conclusion, the establishment of a megamon-

soonal circulation for Pangaea (cf. Kutzbach and of a megamonsoonal circulation, which may have

caused seasonal alternation of flow directionsGallimore, 1989; Parrish, 1993) off ers a plausible

mechanism for seasonally changing directions of within the Corridor.


15/21


Acknowledgements Meleagrinella papyria (Quenstedt): shell

orthocline, ribs relatively widely spaced.

I wish to thank Bill Hay, Axel von Hillebrandt, 1Meleagrinella substriata ( Münster): shell proso-

Wolfgang Kiessling and Dave Lazarus for critically cline, with numerous strong radial ribs.

Terquemia arietis (Quenstedt): attachment areareading the manuscript, and Gerd Westermann

of right valve relatively large.and an anonymous reviewer for their constructive

Terquemia pectiniformis (Eudes-Deslongchamps):reviews. This study was financially supported by a

attachment area of right valve relatively small.grant from the Deutsche Forschungsgemeinschaft

1Placunopsis striatula (Oppel ): includes all radi-(Ab 109/ 1-1), which is acknowledged with

ally ribbed nominal species of Early Jurassicgratitude.Placunopsis.

Propeamussium laeviradiatum (Waagen): dorsal

margins of right valve extended into horn-likeAppendix A: Definition of morphotypes of Early processes, left valve coarsely ribbed.Jurassic pectinoid bivalves occurring in NW-Europe, 1Propeamussium pumilum (de Lamarck): dorsalthe western Tethys and the eastern palaeo-Pacific margins of right valve extended slightly beyond

margin hinge line, left valve finely ribbed.Propeamussium patriciae Poulton: shell large, with

axa marked with an asterisk are known from both radial ornament present on both valves.ends of the Hispanic Corridor. Note that the Kolymonectes carlottensis ( Whiteaves): rightdefinition of morphotypes of European Jurassic valve with relatively broad ribs.pectinids and propeamussiids corresponds to the Kolymonectes coloradoensis ( Weaver): right valvespecies concept of Johnson (1984). with very fine radial striae.

Otapiria inaequicostata Geyer: shell sub-orbicu- 1Entolium lunare (Roemer): small byssal notchlar, left valve ornamented with ribs of diff erent present in juveniles.orders of strength. 1Entolium corneolum (Young and Bird): byssalOtapiria neuquensis Damborenea: shell sub-ovate, notch absent.

radial ornament similar on both valves. Posidonotis semiplicata ( Hyatt): includes all mate-Otapiria pacifica Covacevich and Escobar: shell rial referable to this genus.elongated, ornament stronger on right valve than Agerchlamys wunschae (Marwick): ornament of on left valve. radial riblets and commarginal lamellae, whichOtapiria tailleuri Imlay: shell elongated, radial give rise to a reticulate pattern.ornament more or less equally developed on 1Camptonectes auritus (Schlotheim): sub-orbicu-both valves. lar disc, fine divaricate striae on all parts of disc.Lupherella boechiformis (Hyatt): includes all 1Camptonectes subulatus (Münster): sub-orbicu-material referable to this genus. lar disc, fine divaricate striae restricted to anteriorAnningella carixensis (Cox): includes all material and posterior margins of disc.referable to this genus. Camptonectes obscurus (J. Sowerby): ornament

Oxytoma calva (Schlönbach): shell smooth or consisting of radial striae and commarginal lamel-very weakly ribbed. lae, striae restricted to within a few centimetres

1Oxytoma inequivalvis (J. Sowerby): left valve of the umbo.with moderately high number of well-developed Camptonectes (Costicamptonectes): refers to

primary ribs and intercalated secondary ribs. Camptonectes (Costicamptonectes) sp. A in

1Oxytoma cygnipes (Young and Bird): left valve Aberhan (1998a).

with small number of spinose ribs. Canadonectites paucicostatus Aberhan: right and

Arctotis? frenguellii Damborenea: includes this left valve smooth except for fine radial riblets on

antero-dorsal part of right valve.species and Arctotis sp. A in Aberhan (1998a).


16/21


1Chlamys textoria (Schlotheim): imbricate lamel- 1Weyla meeki Damborenea: shell plano-convex to

lae present on the plicae. feebly biconvex, ribs and interspaces of right and

1Chlamys valoniensis (Defrance): ornament lack- left valve triangular in cross-section.

ing on the plicae. Weyla unca (Philippi) : shell clearly biconvex, ribs

Chlamys pollux (d’Orbigny): presence of long and interspaces of right and left valve triangulartubular spines. in cross-section.

1Eopecten abjectus (Phillips): intercalary costae Weyla yukonensis Aberhan: shell biconvex, ribsrapidly gain the same height as original costae, of right valve with more or less flat crests andtwo median costae greatly enlarged and bearing triangular interspaces, ribs of left valve narrow,tubercles. triangular in cross-section and with concaveEopecten hartzi ( Rosenkrantz): ornament on left interspaces.valve diff erentiated into costae and striae, a few

costae are enlarged.

Eopecten spondyloides (Roemer): original costaeAppendix B: Stratigraphic and geographic distri-similar in height, intercalary costae rapidly gainbution of Early Jurassic pectinioid bivalvethe same size as original costae.

morphotypes1Eopecten velatus (Goldfuss): ornament on leftvalve diff erentiated into costae and striae, no

1=NW-Europe; 2=western Tethys; 3=Southenlarged costae.America; 4=North American craton; 5=westernOchotochlamys aequistriata Aberhan: ornamentNorth American terranes. [ ]=occurrenceof radial riblets and commarginal lamellae andassumed. Data based on Aberhan (1994 and refer-folds equally developed on right and left valves.ences cited therein), Aberhan (1998a,b and refer-Ochotochlamys bureiensis Sey: style of ribbing onences cited therein), Arkell (1933), Behmel andleft and right valves diff erent.Geyer (1966), Benecke (1905), Berini (1957),Pseudopecten barbatus (J. Sowerby): long spinesBertuletti (1962), Brauns (1871), Bronn (1836),present on right valve.Chapuis and Dewalque (1853), Cossmann (1903),Pseudopecten dentatus (J. de C. Sowerby): disc

Cox (1928, 1936), Damborenea (1987 andflanks high and vertically striated, down-sulcalreferences cited therein), Damborenea (1996),tongueing of commarginal striae, modal numberDamborenea and González-León (1998 ), Daresteof plicae 17/ 18.de la Chavanne (1920), Dechaseaux (1936), Dubar1Pseudopecten equivalvis (J. Sowerby): disc flanks(1948), Fucini (1920), Gardet and Gérard (1946),low, commarginal striae curvilinear.Gemmellaro (1872–1882), Geyer (1973), GoldfussPseudopecten veyrasensis (Dumortier): vertically(1833, 1835), Hallam (1987), Hölder (1978, 1990),striated disc flanks, down-sulcal tongueing of Johnson (1984), Joly (1936), Kuhn (1935, 1936,commarginal striae, modal number of plicae 14.1938), de Lamarck (1819), Lanquine (1929),Radulonectites sosneadoensis (Weaver): includesLentini (1973), Leymerie (1881), Lissajous (1907– all eastern Pacific forms referable to this genus.1912), Oppel (1853, 1856), Pedersen (1986),Weyla alata (von Buch): shell concave–convex to

Phillips (1829, 1871), Quenstedt (1851–1852,plano-convex, ribs of right valve with almost flat1856–1857, 1865–1866, 1882–1885), Riccardi et al.crests and concave interspaces, ribs of left valve

(1990), Rollier (1915), Schäfle (1929), Schlönbachnarrow and with concave interspaces.(1863), Staesche (1926), Terquem (1855),Weyla ayarti (Dubar): right valve small, with

Terquem and Piette (1865), Troedsson (1951),only up to six subtriangular main ribs.

Vacek (1886), de Verneuil and Collomb (1853),Weyla bodenbenderi (Behrendsen): shell concave–

Zieten (1833) and unpublished information fromconvex, ribs of right and left valve relatively

the Huayacocotla trough in eastern Mexico andbroad, number of ribs increasing by intercalation

and branching. the Antimonio terrane of NW-Mexico.


17/21


Morphotype Hettangian Sinemurian Pliensbachian Toarcian

Otapiria inaequicostata 3

Otapiria neuquensis 3 3

Otapiria pacifica 3 3

Otapiria tailleuri 4Lupherella boechiformis 4, 5

Anningella carixensis 1

Oxytoma calva 1 1

Oxytoma inequivalvis 1, 2, 3, 4, 5 1, 2, 3, 4, 5 1, [2], 3, [4], 5 1, 2, 3, 4, 5

Oxytoma cygnipes 1, 3 1, 4 1, 4, 5 5

Arctotis? frenguellii 4 3

Meleagrinella papyria 1 1

Meleagrinella substriata 1, 5 1, 5 1

Terquemia arietis 1 1 2

Terquemia pectiniformis 1

Placunopsis striatula 1, 2 1, [2], 3, 5 1, [2], 3, 5 1, 2, 3, 4

Propeamussium laeviradiatum 1 1, 2

Propeamussium pumilum 1, 2 1, 2, 3

Propeamussium patriciae 4, 5

Kolymonectes carlottensis 5

Kolymonectes coloradoensis 4 3

Entolium lunare 1, 2 1, 2, 3 1, 2 1, 5

Entolium corneolum 3, 5 3, 4, 5 3, [4], 5 1, 2, 3, 4, 5

Posidonotis semiplicata 4, 5 3, 5 3, 5

Agerchlamys wunschae 3, 4, 5 4, 5 3, 5 5

Camptonectes auritus 1 1, 2 [1], 2, 3 1, 2, 3, 5

Camptonectes subulatus 1, 3 1, [2], 3, 4 1, 2, [4] 1, 2, 4

Camptonectes obscurus 1

Camptonectes (Costicamptonectes) 5

Canadonectites paucicostatus 5 5

Chlamys textoria 1, 2, 3 1, 2, 3, 4, 5 1, 2, 3, 4, 5 1, 2, 3, 5

Chlamys valoniensis 1, 2, 3 1, 3, 4, 5Chlamys pollux 1, 2 1, 2

Eopecten abjectus 1 1, 3

Eopecten hartzi 4, 5 4, 5 3, 4

Eopecten spondyloides 1

Eopecten velatus 1, 2, 3 1, 2, [3] 1, 2, 3 1, 2, 3

Ochotochlamys aequistriata 5 4, 5 4, 5

Ochotochlamys bureiensis 4 4

Pseudopecten barbatus 1, 2

Pseudopecten dentatus 1, 2 [1], 2 1, 2 1, [2]

Pseudopecten equivalvis 1, 2 1, 2 1, 2, 3 1, 2, 3

Pseudopecten veyrasensis 1, 2 [1], [2] 1, 2

Radulonectites sosneadoensis 3, 4, 5

Weyla alata 4 3, 4, 5 3, 4, 5 3

Weyla ayarti 2Weyla bodenbenderi 3, 5 3, 5 3, 5

Weyla meeki 4 4, 5 2, 5 2

Weyla unca 4 3, 4, 5 3, 5 3

Weyla yukonensis 5 4, 5


18/21


Brauns, D., 1871. Der untere Jura im nordwestlichen Deutsch-Referencesland von der Grenze der Trias bis zu den Amaltheenthonen

mit besonderer Berücksichtigung seiner Molluskenfauna.Aberhan, M., 1993. Benthic macroinvertebrate associations on

Vieweg & Sohn Braunschweig. 493 pp.a carbonate-clastic ramp in segments of the Early Jurassic

Bronn, H.G., 1836. In: Lethaea geognostica. Schweizerbart,back-arc basin of northern Chile (26–29°S). Rev. Geol.

Stuttgart pp. 225–480.

Chile 20, 105–136. Chandler, M.A., Rind, D., Ruedy, R., 1992. Pangaean climateAberhan, M., 1994. Early Jurassic Bivalvia of northern Chile.

during the Early Jurassic: GCM simulations and the sedi-Part I. Subclasses Palaeotaxodonta, Pteriomorphia and

mentary record of paleoclimate. Geol. Soc. Am. Bull. 104,Isofilibranchia. Beringeria 13, 3–115.

543–559.Aberhan, M., 1998a. Early Jurassic Bivalvia of western Canada.

Chapuis, F., Dewalque, C., 1853. Description des fossiles desPart I. Subclasses Palaeotaxodonta, Pteriomorphia and

terraines secondaires de la province de Luxembourg. Mem.Isofilibranchia. Beringeria 21, 57–150.

Acad. R. Belge 35 303 pp.Aberhan, M., 1998b. Paleobiogeographic patterns of pectinoid

Cossmann, M., 1903. Note sur L’Infralias de la Vendée et desbivalves and the Early Jurassic tectonic evolution of western

Deux Sèrres. II. Pélécypodes. Bull. Soc. Géol. Fr., Sér. 4Canadian terranes. Palaios 13, 129–148.

3, 497–545.Aberhan, M., 1999. Terrane history of the Canadian Cordillera:

Cox, L.R., 1928. The Belemnite Marls of Charmouth, a seriesestimating amounts of latitudinal displacement and rotation

in the Lias of the Dorset Coast. VI. Gastropod and Lamelli-of Wrangellia and Stikinia. Geol. Mag. 136, 481–492.

branch Molluscs. Q. J. Geol. Soc. London 84, 233–245.Aberhan, M., Fürsich, F.T., 1997. Diversity analysis of Lower

Cox, L.R., 1936. The Gastropoda and Lamellibranchia of theJurassic bivalves of the Andean Basin and the Pliensbachian-Green Ammonite Beds of Dorset. Q. J. Geol. Soc. London

–Toarcian mass extinction. Lethaia 29, 181–195.92, 456–471.

Aberhan, M., Fürsich, F.T., 2000. Mass origination versus massCreber, G.T., Chaloner, W.G., 1984. Influence of environmen-

extinction: the biological contribution to the Pliensbachian-tal factors on the wood structure of living and fossil trees. –Toarcian extinction event. J. Geol. Soc. London 157,Bot. Rev. 50, 357–448.55–60.

Crowley, T.J., North, G.R., 1991. Paleoclimatology. OxfordAberhan, M., Hillebrandt, A.v., 1999. The bivalve Opisoma inMonogr. Geol. Geophys. 18, 1–349.the Lower Jurassic of northern Chile. Profil 16, 149–164.

Damborenea, S.E., 1987. Early Jurassic Bivalvia of Argentina.Aberhan, M., Pálfy, J., 1996. A low oxygen tolerant East PacificPart 2. Superfamilies Pteriacea, Buchiacea and part of Pecti-flat clam (Posidonotis semiplicata) from the Lower Jurassicnacea. Palaeontographica ( A) 199, 113–216.of the Canadian Cordillera. Can. J. Earth Sci. 33, 993–1006.

Damborenea, S.E., 1993. Early Jurassic South American pecti-Arkell, W.J., 1933. A monograph of British Corallian Lamelli-naceans and circum-Pacific palaeobiogeography. Palaeo-branchia. Monogr. Palaeontogr. Soc. London 5, 181–228.geogr., Palaeoclimatol., Palaeoecol. 100, 109–123.Baker, P.G., Manceñido, M.O., 1997. The morphology and

Damborenea, S.E., 1996. Palaeobiogeography of Early Jurassicshell microstructure of the thecideidine brachiopod Ancorel-bivalves along the southeastern Pacific margin. In: XIIIlina ageri from the Lower Jurassic of Argentina. Palaeon-Congreso Geológico Argentino and III Congreso de Explor-tology 40, 191–200.ación de Hidrocarburos Actas 5, 151–167.Barron, E.J., Harrison, C.G.A., Sloan II, J.L., Hay, W.W.,

Damborenea, S.E., 2000. Hispanic Corridor: its evolution and1981. Paleogeography, 180 million years ago to present.the biogeography of bivalve molluscs. In: Hall, R.L., Smith,Eclog. Geol. Helv. 74, 443–470.P.L. (Eds.), Advances in Jurassic Research 2000, GeoRes.Behmel, H., Geyer, O.F., 1966. Beiträge zur Stratigraphie undForum 6, 369–380.Paläontologie des Juras von Ostspanien. III. Stratigraphie

Damborenea, S.E., Gonzaláz-León, C.M., 1998. Late Triassicund Fossilführung im Unterjura von Albarracin (Provinzand Early Jurassic bivalves from Sonora, Mexico. Rev. Mex.Teruel). N. Jb. Geol. Paläont. Abh. 124, 1–52.Cienc. Geol. 14, 178–201.Benecke, E.W., 1905. Die Versteinerungen der Eisenerzforma-

Damborenea, S.E., Manceñido, M.O., 1979. On the palaeogeo-tion von Deutsch-Lothringen und Luxemburg. Abh. Geol.graphical distribution of the pectinid genus Weyla (Bivalvia,Spez.-Karte von Elsaß-Lothringen, N.F. 6, 1–598.

Lower Jurassic). Palaeogeogr., Palaeoclimatol., Palaeoecol.Berini, L., 1957. Studi paleontologici sul Lias del Monte27, 85–102.Albenza (Bergamo). Lamellibranchi e gastropodi del Lias

Damborenea, S.E., Manceñido, M.O., 1988. Weyla: Semblanzainferiore. Riv. Ital. Paleont. Stratigr. 63, 31–64.de un bivalvo Jurasico Andino. In: V Congreso GeologicoBertuletti, C., 1962. Studi paleontologici sul Lias del MonteChileno Tomo 2., C13–C15.Albenza (Bergamo). I lamellibranchi dell’ Hettangiano. Riv.

Damborenea, S.E., Manceñido, M.O., 1992. A comparison of Ital. Paleont. Stratigr. 68, 169–192.Jurassic marine benthonic faunas from South America andBoomer, I., Ballent, S., 1996. Early–Middle Jurassic ostracod

New Zealand. J. R. Soc. N.Z. 22, 131–152.migration between the northern and southern hemispheres:

Damborenea, S.E., Polubotko, I.V., Sey, I.I., Paraketsov, K.V.,further evidence for a proto Atlantic–Central America con-

1992. Bivalve zones and assemblages of the circum-Pacificnection. Palaeogeogr., Palaeoclimatol., Palaeoecol. 121,

53–64. region. In: Westermann, G.E.G. (Ed.), The Jurassic of the


19/21


Circum-Pacific. Cambridge University Press, Cambridge, Hallam, A., 1994. An outline of phanerozoic biogeography.

Oxford Biogeogr. Ser. 10, 1–246.pp. 300–307.

Dareste de la Chavanne, J., 1920. Fossiles liasiques de la région Hallam, A., 1998. The determination of Jurassic environments

using palaeoecological methods. Bull. Soc. Géol. Fr. 169,de Guelma. Matér. Carte Géol. Algér., Sér. 1 (Paléont.)

5 72 pp. 681–687.

Hay, W.W., Behensky, J.F., Barron, E.J., Sloan II, J.L., 1982.Dechaseaux, C., 1936. Pectinidés jurassiques de l’est du Bassin

de Paris. Révision et biogéographie. Ann. Palèont. 25, Late Triassic–Liassic paleoclimatology of the proto-centralNorth Atlantic rift system. Palaeogeogr., Palaeoclimatol.,1–148.

de Lamarck, J.B, 1819. Histoire naturelle des animaux sans Palaeoecol. 40, 13–30.

Hayami, I., 1975. A systematic survey of the Mesozoic Bivalviavertebres Tome 6. Verdière. 343 pp.

de Verneuil, M., Collomb, E., 1853. Coup d’oeil sur la constitu- from Japan. Univ. Mus., Univ. Tokyo, Bull. 10, 1–249.

Hillebrandt, A.v., 1973. Die Ammonitengattungen Bouleicerastion géologique de quelques provinces de l’Espagne. Bull.

Soc. Géol. Fr. Paris, Sér. 2 10, 61–147, 162–166. und Frechiella im Jura von Chile und Argentinien. Eclog.

Geol. Helv. 66, 351–363.Dubar, G., 1948. Études paléontologiques sur le Lias du Maroc.

La faune Domérienne du Djebel Bou-Dahar. Notes Mém. Hillebrandt, A.v., 1981. Kontinentalverschiebung und die

paläozoogeographischen Beziehungen des südamerikan-Serv. Géol. Maroc 68, 1–250.

Efimova, A.F., Kinasov, V.P., Paraketsov, K.V., Polubotko, ischen Lias. Geol. Rdsch. 70, 570–582.

Hillebrandt, A.v., Schmidt-Effing, R., 1981. Ammoniten ausI.V., Repin, Yu.S., Dagis, A.S., 1968. Field atlas of the Jur-

assic fauna and flora of the northeastern part of the USSR. dem Toarcium (Jura) von Chile (Südamerika). Zitteliana

6, 1–74.Ministry of Geology RSFSR, Severo-vostochnoye ordenatrydovogo krasnogo Znameni geologicheskoe upravlenie, Hölder, H., 1978. Ü ber die Pectiniden-Gattung Parvamussium

im Jura. Stutt. Beitr. Naturk., Ser. B 38 37 pp.Magadanskoe Knizhnoe-Izdatel’stvo, 378 pp. (in Russian).

Fucini, A., 1920. Fossili domeriani dei dintorni di Taormina. Hölder, H., 1990. Ü ber die Muschelgattung Placunopsis (Pecti-

nacea, Placunopsidae) in Trias und Jura. Stutt. Beitr.Parte I. Palaeontogr. Ital. 26, 75–116.

Fürsich, F.T., 1993. Palaeoecology and evolution of Mesozoic Naturk., Ser. B 165 63 pp.

Jakobs, G.K., 1995. New occurrences of Leukadiella and Paro-salinity-controlled benthic macroinvertebrate associations.

Lethaia 26, 327–346. niceras (Ammonoidea) from the Toarcian (Lower Jurassic)

of the Canadian Cordillera. J. Paleont. 69, 89–98.Gardet, G., Gérard, C., 1946. Contribution a l’étude paléon-

tologique du Moyen-Atlas septentrional. Notes Mém. Serv. Jeletzky, J.A., 1980. Dicoelitid belemnites from the Toarcian–

Middle Bajocian of western and Arctic Canada. Geol. Surv.Géol. Maroc 64, 1–88.

Gemmellaro, G.G., 1872–1882. Sopra alcune faune giuresi e Can. Bull. 338, 1–71.

Johnson, A.L.A., 1984. The palaeobiology of the bivalve fami-liasiche della Sicilia. Studi paleontologici. Lao. Palermo,

434 pp. lies Pectinidae and Propeamussiidae in the Jurassic of

Europe. Zitteliana 11, 1–235.Geyer, O.F., 1973. Das präkretazische Mesozoikum von

Kolumbien. Geol. Jb. B 5 155 pp. Joly, H., 1936. Les fossiles du Jurassique de la Belgique avec

description stratigraphique de chaque étage. DeuxièmeGoldfuss, G.A., 1833. In: Petrefacta Germaniae. II (1). Arnz,

Düsseldorf, pp. 1–68. partie. Lias inférieur. Mém. Mus. R. Hist. Nat. Belg. 79,

1–244.Goldfuss, G.A., 1835. In: Petrefacta Germaniae. II (2). Arnz,

Düsseldorf, pp. 69–140. Kristan-Tollmann, E., Tollmann, A., 1982. Die Entwicklung

der Tethystrias und Herkunft ihrer Fauna. Geol. Rdsch.Gradstein, F.M., Agterberg, F.P., Ogg, J.G., Hardenbol, J., van

Veen, P., Thierry, J., Huang, Z., 1994. A Mesozoic time 71, 987–1019.

Kuhn, O., 1935. Weitere Beiträge zur Fauna des untersten Liasscale. J. Geophys. Res. 99, 24,051–24,074.

Hallam, A., 1977. Jurassic bivalve biogeography. Paleobiology in Schwaben und Franken. Jb. Ver. Vaterländ. Naturk.

Württ. 91, 2–18.3, 58–73.

Hallam, A., 1983. Early and mid-Jurassic molluscan biogeogra- Kuhn, O., 1936. Die Fauna des Amaltheentons (Lias ∂) in Fran-

ken. N. Jb. Min. Geol. Paläont. B 75, 231–311.phy and the establishment of the central Atlantic seaway.

Palaeogeogr., Palaeoclimatol., Palaeoecol. 43, 181–193. Kuhn, O., 1938. Die Fauna des Dogger ∂ der Frankenalb (MitNachträgen zum übrigen Jura). Nova Acta Leopold. N.F.Hallam, A., 1987. Radiations and extinctions in relation to envi-

ronmental change in the marine Lower Jurassic of northwest 6, 125–170.

Kutzbach, J.E., Gallimore, R.G., 1989. Pangaean climates:Europe. Paleobiology 13, 152–168.

Hallam, A., 1988. A reevaluation of Jurassic eustasy in the light megamonsoons of the megacontinent. J. Geophys. Res. 94,

3341–3357.of new data and the revised Exxon curve. In: Wilgus, C.K.,

Hastings, B.S.Posamentier, H., Wagoner, J.V., Ross, C.A., Lanquine, A., 1929. Le Lias et le Jurassique des chaines

provençales. I. Le Lias et le Jurassique Inférieur. Bull. Serv.Kendall, C.G.S.C. (Eds.), Sea-level Changes — An Integ-

rated Approach, SEPM Spec. Publ. 42, 261–273. Carte Géol. Fr. 32, 41–425.

Lentini, F., 1973. I molluschi del Lias inferiore di Lorigi (SiciliaHallam, A., 1992. Phanerozoic Sea-Level Changes. Columbia

University Press, Columbia. nordorientale). Boll. Soc. Paleont. Ital. 12, 23–75.


20/21


Leymerie, A., 1881. Description géologique et paléontologique of the Circum-Pacific. Cambridge University Press, Cam-

bridge, pp. 365–379.des Pyrénées de la Haute-Garonne. Édouard Privat.

Toulouse 1010 pp. Parrish, J.T., 1993. Climate of the supercontinent Pangea.

J. Geol. 101, 215–233.Lissajous, M., 1907–1912. Jurassique Maconnais. Description

des fossiles caractéristiques et des espèces les plus commu- Parrish, J.T., Ziegler, A.M., Scotese, C.R., 1982. Rainfall pat-

terns and the distribution of coals and evaporites in thenes. Bull. Soc. Hist. Nat. Macon 3 496 pp.

Liu, C., Heinze, M., Fürsich, F.T., 1998. Bivalve provinces Mesozoic and Cenozoic. Palaeogeogr., Palaeoclimatol.,Palaeoecol. 40, 67–101.in the Proto-Atlantic and along the southern margin of

the Tethys in the Jurassic. Palaeogeogr., Palaeoclimatol., Pedersen, G.K., 1986. Changes in the bivalve assemblage of an

Early Jurassic mudstone sequence (the Fjerritslev Forma-Palaeoecol. 137, 127–151.

Loriga, C., Neri, C., 1976. Aspetti paleobiologici e paleogeo- tion in the Gassum 1 Well, Denmark). Palaeogeogr., Palaeo-

climat., Palaeoecol. 53, 139–160.grafici della facies a ‘Lithiotis’ (Giurese Inf.). Riv. Ital.

Paleont. Stratigr. 82, 651–706. Phillips, J., 1829. Illustrations of the Geology of Yorkshire.

Wilson and Sons, York. 199 pp.Manceñido, M.O., Dagys, A.S., 1992. Brachiopods of the

circum-Pacific region. In: Westermann, G.E.G. (Ed.), The Phillips, J., 1871. Geology of Oxford and the Valley of the

Thames. Clarendon Press, Oxford. 523 pp.Jurassic of the Circum-Pacific. Cambridge University Press,

Cambridge, pp. 328–333. Polubotko, I.V., Repin, Yu.S., 1988. Lower and Middle Jurassic

of the North-East. In: Westermann, G.E.G., Riccardi, A.C.Manceñido, M.O., Damborenea, S.E., 1990. Corallophilous

micromorphic brachiopods from the Lower Jurassic of west (Eds.), Jurassic Taxa Ranges and Correlation Charts for

the Circum Pacific. 1. Soviet Union, Newslett. Stratigr. 19,central Argentina. In: MacKinnon, D.I., Lee, D.E., Camp-bell, J.D. (Eds.), Brachiopods through Time. Balkema, Rot- 1–17.

Quenstedt, F.A., 1851–1852. Handbuch der Petrefaktenkunde.terdam, pp. 89–96.

McKenna, M.C., 1973. Sweepstakes, filters, corridors, Noah’s first ed., Laupp and Siebeck. Tübingen 792 pp.

Quenstedt, F.A., 1856–1857. Der Jura. Tübingen Laupp.arks, and beached Viking funeral ships in palaeogeography.

In: Tarling, D.H., Runcorn, S.K. (Eds.), Implications of 842 pp.

Quenstedt, F.A., 1865–1866. Handbuch der Petrefaktenkunde.Continental Drift to the Earth Sciences. Academic Press,

New York, pp. 295–308. second ed., Laupp and Siebeck. Tübingen 982 pp.

Quenstedt, F.A., 1882–1885. Handbuch der Petrefaktenkunde.Milova, L.V., 1976. Stratigraphy and bivalve molluscs of the

Triassic–Jurassic deposits of northern Priokhotya. Akade- third ed., Laupp. Tübingen 1239 pp.

Riccardi, A.C., 1991. Jurassic and Cretaceous marine connec-miya Nauk SSSR, Dal’nevostochnyy Nauchnyy Tsentr,

Trudy Severo-Vostochnyy Kompleksnyy Nauchno-Issledo- tions between the Southeast Pacific and Tethys. Palaeo-

geogr., Palaeoclimatol., Palaeoecol. 87, 155–189.vatel’-skiy Instituta 65, pp. 3–110 (in Russian).

Milova, L.V., 1985. New Pliensbachian bivalve molluscs of Riccardi, A.C., Damborenea, S.E., Manceñido, M.O., 1990.

Lower Jurassic of South America and Antarctic Peninsula.North Priokhotya. In: Bivalve and Cephalopod Mollusks

of the North-East of the USSR. Akademiya Nauk SSSR, Newslett. Stratigr. 21, 75–103.

Rollier, L., 1915. Fossiles nouveaux ou peu connus des terrainspp. 42–56. in Russian.

Milova, L.V., 1988. Early Jurassic bivalve molluscs of north- secondaires (mésozoiques) du Jura et des contrées envi-

ronnantes. Mém. Soc. Paléont. Suisse 41, 345–500.eastern USSR. Akademiya Nauk SSSR, Dal’nevostochnyy

Otdeleniye, Trudy Severo-Vostochnyy Kompleksnyy Sandy, M.R., Stanley Jr., G.D., 1993. Late Triassic brachiopods

from the Luning Formation, Nevada, and their palaeobio-Nauchno-Issledovatel’-skiy Instituta, 152 pp. (in Russian).

Nauss, A.L., Smith, P.L., 1988. Lithiotis (Bivalvia) bioherms in geographical significance. Palaeontology 36, 439–480.

Schäfle, L., 1929. Ü ber Lias- und Doggeraustern. Geol. Paläont.the Lower Jurassic of east-central Oregon, USA. Palaeo-

geogr., Palaeoclimatol., Palaeoecol. 65, 253–268. Abh. N.F. 17, 63–150.

Schlönbach, U., 1863. Ueber den Eisenstein des mittleren LiasNewton, C.R., 1988. Significance of ‘Tethyan’ fossils in the

American Cordillera. Science 242, 385–391. im nord-westlichen Deutschland, mit Berücksichtigung der

älteren und jüngeren Lias-Schichten. Zeitschr. dt. Geol. Ges.Olsen, P.E., 1997. Stratigraphic record of the Early Mesozoic

breakup of Pangea in the Laurasia–Gondwana rift system. 15, 465–566.Schmidt-Effing, R., 1980. The Huayacocotla aulacogen inAnnu. Rev. Earth Planet. Sci. 25, 337–401.

Oppel, A., 1853. Der mittlere Lias Schwabens. Jh. Ver. Vater- Mexico (Lower Jurassic) and the origin of the Gulf

of Mexico. In: Pilger, R.H. (Ed.), The Origin of the Gulf of länd. Naturk. Württ. 10, 39–136.

Oppel, A., 1856. Die Juraformation Englands, Frankreichs und Mexico and the Early Opening of the Central North Atlantic

Ocean. LouisianaState University, Baton Rouge, pp. 79–86.des südwestlichen Deutschlands. Württ. Naturwiss. Jh. 12,

1–438. Sey, I.I., 1984. The Late Pliensbachian bivalves of Bureya

Trough (Far East of Russia). In: Poyarkova, Z.N., Zonova-Palmer, C.P., 1989. Larval shells of four Jurassic bivalve mol-

luscs. Bull. Br. Mus. Nat. Hist. (Geol.) 45, 57–69. lov, V.P. (Eds.), New Data on the Detailed Biostratigraphy

of the Phanerozoic of the Far East. Akademiya Nauk SSSR,Parrish, J.T., 1992. Jurassic climate and oceanography of the

Pacific region. In: Westermann, G.E.G. (Ed.), The Jurassic pp. 86–97. in Russian.


21/21


Simpson, G.G., 1940. Mammals and land bridges. J. Wash- (Rhaeto-Lias). Lunds Univ. Arsskrift, N.F. Avd. 2 (47) ,

1–268.ington Acad. Sci. 30, 137–163.

Smith, P.L., 1983. The Pliensbachian ammonite Dayiceras day- Vacek, M., 1886. Ü ber die Fauna der Oolithe von Cap. S. Vigi-

lio verbunden mit einer Studie über die obere Liasgrenze.iceroides and Early Jurassic paleogeography. Can. J. Earth

Sci. 20, 86–91. Abh. k. k. Geol. Reichsanst. 12, 1–212.

van Andel, T.H., 1994. New Views on an Old Planet. Cam-Smith, P.L., 1988. Paleobiogeography and plate tectonics.

Geosci. Can. 15, 261–279. bridge Univerity Press, Cambridge. 439 pp.Waller, T.R., 1991. Evolutionary relationships among commer-Smith, P.L., Tipper, H.W., 1986. Plate tectonics and paleobioge-

ography: Early Jurassic (Pliensbachian) endemism and cial scallops (Mollusca: Bivalvia: Pectinidae). In: Shumway,

S.E. ( Ed.), Scallops: Biology, Ecology and Aquaculture.diversity. Palaios 1, 399–412.

Smith, P.L., Westermann, G.E.G., Stanley, G.D., Yancey, T.E., Elsevier, Amsterdam, pp. 1–73.

Waller, T.R., 1993. The evolution of ‘Chlamys’ ( Mollusca:1990. Paleobiogeography of the ancient Pacific. Science

249, 680–681. Bivalvia: Pectinidae) in the tropical western Atlantic and

eastern Pacific. Am. Malacol. Bull. 10, 195–249.Staesche, K.v., 1926. Die Pectiniden des Schwäbischen Jura.

Geol. Paläont. Abh. N.S. 15 136 pp. Westermann, G.E.G., 1977. Comments to Hallam’s conclusion

regarding the first marine connection between the easternStanley Jr., G.D., 1994. Late Paleozoic and early Mesozoic reef-

building organisms and paleogeography: the Tethyan– Pacific and western Tethys. In: West, R.M. (Ed.), Paleontol-

ogy and Plate Tectonics, Milwaukee Publ. Mus. Spec. Publ.North American connection. Cour. Forsch.-Inst. Senckenb-

erg 172, 69–75. Biol. Geol. 2, 35–38.

Westermann, G.E.G., 1993. Global bio-events in mid-JurassicStanley Jr., G.D., Beauvais, L., 1994. Corals from an EarlyJurassic coral reef in British Columbia refuge on an oceanic ammonites controlled by seaways. In: House, M.R. (Ed.),

The Ammonoidea: Environment, Ecology and Evolutionaryisland reef. Lethaia 27, 35–47.

Terquem, O., 1855. Paléontologie de l’étage inférieur de la for- Change, System. Assoc. Spec. Vol. 47, 187–226.

Westermann, G.E.G., Riccardi, A., 1985. Middle Jurassicmation liasique de la province de Luxembourg, Grand-

Duché (Hollande) et de Hettange, du Département de la ammonite evolution in the Andean Province and emigration

to Tethys. In: Bayer, U., Seilacher, A. (Eds.), SedimentaryMoselle. Mém. Soc. Géol. Fr., Sér. 2 5, 219–343.

Terquem, O., Piette, E., 1865. Le Lias inférieur de l’est de la and Evolutionary Cycles. Springer, Berlin, pp. 4–34.

Ziegler, A.M., Parrish, J.M., Yao, J., Gyllenhaal, E.D., Rowley,France comprenant la Meurthe, la Moselle, le Grand-Duché

de Luxembourg, la Belgique et la Meuse. Mém. Soc. Géol. D.B., Parrish, J.T., Nie, S., Bekker, A., Hulver, M.L., 1993.

Early Mesozoic phytogeography and climate. Philos. Trans.Fr., Sér. 2 8, 1–175.

Trechmann, C.T., 1923. The Jurassic rocks of New Zealand. Q. R. Soc. London, Ser. B: 341, 297–305.

Zieten, C.H.v., 1833. In: Die Versteinerungen Württembergs.J. Geol. Soc. London 79, 246–312.

Troedsson, G., 1951. On the Höganäs Series of Sweden Schweizerbart Stuttgant, pp. 65–102.

aberhan (2001) -- bivalve palaeobiogeography n' the hispanic corridor-time of opening

Documents