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Cretaceous Research 29 (2008) 217e236www.elsevier.com/locate/CretRes

Lateral lithological and compositional variations of theCretaceous/Tertiary deep-sea tsunami deposits in northwestern Cuba

Kazuhisa Goto a,*, Ryuji Tada a, Eiichi Tajika a, Manuel A. Iturralde-Vinent b,Takafumi Matsui c, Shinji Yamamoto a, Yoichiro Nakano a, Tatsuo Oji a, Shoichi Kiyokawa d,

Dora E. Garcıa Delgado e, Consuelo Dıaz Otero f, Reinaldo Rojas Consuegra b

a Department of Earth and Planetary Science, Building #5, Graduate School of Science, The University of Tokyo, 7-3-1 Hongo, Tokyo 113-0033, Japanb Museo Nacional de Historia Natural, Obispo No. 61, Plaza de Armas, La Habana Vieja 10100, Cuba

c Department of Complexity Science and Engineering, Graduate School of Frontier Science, The University of Tokyo, 7-3-1 Hongo, Tokyo 113-0033, Japand Department of Earth and Planetary Sciences, Faculty of Sciences, Kyushu University, 33 Hakozaki, Fukuoka 812-8581, Japan

e Centro de Investigaciones del Petroleo, Washington No. 166, esquina Churruca, Municipio Cerrro, Ciudad de La Habana, Cubaf Instituto de Geologıa y Paleontologıa, Vıa Blanca y Lınea del Ferrocarril, San Miguel del Padron, La Habana 11 000, Cuba

Received 8 June 2006; accepted in revised form 28 April 2007

Available online 17 November 2007

Abstract

Lateral lithological, compositional, and grain size variations in the Pe~nalver Formation in northwestern Cuba, which is a Cretaceous/Tertiary(K/T) boundary deposit accumulated on the northwestern slope of the extinct Cretaceous Cuban arc and distributed over an area of 150 km, areexamined in order to investigate the influence of a tsunami on the deep-sea bed. The lower part of the Pe~nalver Formation is composed ofcalcirudite containing grains derived from a shallow platform. It is considered to have been deposited by debris flows from the shallow carbonateplatform triggered by the impact of the seismic wave. The upper part of the formation is composed of calcarenite to calcilutite hemipelagic topelagic sediments. This has a distinctly different source to the lower part and is considered as having been formed under the influence of tsunamiwaves, judging from its regional homogeneity and the presence of serpentine lithic grains that were probably transported from central to easternCuba by a westward flowing water mass. An erosional surface between the two parts, together with sedimentary structures in the upper partindicative of current influence is more common with decreasing presumed depositional depth, which can be interpreted as stronger tsunami ef-fect at the shallower depths. In addition, compositional and grain size oscillations that repeated >6 to 10 times are observed in the upper part,which may reflect repeated lateral injection of the sediments eroded from the shelf to the upper slope of the depositional basin by backwash ofsuccessive tsunami waves into the dense sediment suspended cloud that was formed by the first tsunami.� 2007 Elsevier Ltd. All rights reserved.

Keywords: Cretaceous/Tertiary boundary; Impact event; Tsunami deposit; Pe~nalver Formation; Cuba

1. Introduction

A large number of tsunami deposits have been reportedfrom both outcrops and drill cores, and sediment transporta-tion mechanisms induced by the tsunami have been

* Corresponding author. Present address: Disaster Control Research Center,

Graduate School of Engineering, Tohoku University, Aoba 06-6-11, Aramaki,

Sendai 980-8579, Japan.

E-mail address: [email protected] (K. Goto).

0195-6671/$ - see front matter � 2007 Elsevier Ltd. All rights reserved.

doi:10.1016/j.cretres.2007.04.004

investigated to evaluate the magnitude and generation of thepast tsunamis (e.g. Atwater, 1987; Minoura and Nakaya,1991; Kelsey et al., 2005). However, few studies have exam-ined the influence and sediment transport mechanisms of tsu-nami on the deep-sea floor, because lithological characteristicsof deep-sea tsunami deposits are not well understood. One ex-ample of a deep-sea deposit with strong evidence of a tsunamiorigin is reported from the Mediterranean Sea (Kastens andCita, 1981; Cita et al., 1996; Cita and Aloisi, 2000). It hasbeen shown that a large tsunami was generated by the eruption

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218 K. Goto et al. / Cretaceous Research 29 (2008) 217e236

of the Santorini volcano at approximately 3500 yr BP, anddeep sea sediments are coeval with this event (Kastens andCita, 1981). Kastens and Cita (1981) termed the deep seadeposit a homogenite, and interpreted it as a tsunami depositbased on (1) thick and massive appearance with monotonicupward fining, (2) grains of hemipelagic to pelagic origin,(3) absence of primary depositional structures, (4) absenceof bioturbation, and (5) presence of the homogenite in thenon-seismic area. However, the depositional mechanism ofthe homogenite is still uncertain, because it has only beensampled in piston cores, making it difficult to investigate thelateral and vertical lithological characteristics of the depositin detail. Furthermore, it is uncertain whether all deep-sea tsu-nami deposits have features similar to the Santorini-generatedhomogenite, and whether or not there is significant lateral lith-ological variations which relate to changes in depositionaldepth and/or tsunami magnitude.

The impact of an extraterrestrial object into the ocean is onemechanism for generating a gigantic tsunami (e.g. Jansa, 1993;Ormo and Lindstrom, 2000; Gersonde et al., 2002; Dypvik andJansa, 2003). For example, large tsunamis are believed to havebeen generated by the Chicxulub impact at the Cretaceous/Tertiary (K/T) boundary (e.g., Matsui et al., 2002). Severalprobable K/T boundary tsunami deposits have been reportedaround the Gulf of Mexico (e.g. Bourgeois et al., 1988; Alvarezet al., 1992; Smit et al., 1992, 1996; Smit, 1999; Lawton et al.,2005; Schulte et al., 2006), the proto-Caribbean sea (Maurrasseand Sen, 1991; Takayama et al., 2000; Tada et al., 2002, 2003),and in the Chicxulub crater (Goto et al., 2004).

Pszczolkowski (1986) investigated the Pe~nalver Formationin northwestern Cuba, an upward fining unit (Bronnimann andRigassi, 1963; Iturralde-Vinent, 1992), and suggested that itwas probably related to the K/T boundary impact. This pro-posal was later supported by Takayama et al. (2000) basedon the biostratigraphy and the presence of impact-related ma-terials. Takayama et al. (2000) interpreted the lower part of thePe~nalver Formation as a gravity flow deposit triggered by theimpact seismic wave, whereas the upper part was interpretedas a deep-sea tsunami deposit because of the similarity ofthe sedimentary features to those of the Santorini-generatedhomogenite in the Mediterranean Sea. However, their studywas based on observations at only one locality with low-resolution analyses.

The Pe~nalver Formation is 180 m thick and widely distrib-uted, thus high-resolution analyses are possible. In this study,the lateral and vertical lithological variations of the Pe~nalverFormation are examined to test the tsunami origin of the upperpart and to evaluate the effect of changes in depositional depthand/or tsunami magnitude on lithology. In addition, high res-olution petrographical, mineralogical, and grain size analyseswere conducted to clarify its depositional mechanism.

2. Geological setting

The Cuban foldbelt is composed of five tectonic units(Iturralde-Vinent, 1994, 1998): (1) Bahamian platform andborderland, (2) allochthonous Cuban SW terranes, (3)

allochthonous Northern ophiolite belt, (4) allochthonousCretaceous island arc complex (¼an extinct Cretaceous Cubanarc), and (5) Paleogene volcanic arc of southeastern Cuba.

The extinct Cretaceous Cuban arc is in tectonic contactabove the Bahamian platform and Northern ophiolites belt inthe north. It is composed of a deformed and partially metamor-phosed arc complex of Aptian to Campanian age, which inturn is overlain by a system of post-arc latest Campanianthrough Paleogene sedimentary basins, some of which includea K/T boundary section (Iturralde-Vinent, 1994, 1998;Iturralde-Vinent et al., 2000; Dıaz-Otero et al., 2000; Tadaet al., 2003). In the Late Cretaceous, the extinct CretaceousCuban arc was located 500 to 700 km southesoutheast of itspresent position (Rosencrantz, 1990; Pindell, 1994). In theMaastrichtian, the extinct arc complex was covered by theCuban carbonate platform and several siliciclastic sedimentarybasin units developed both above the arc and on the northernand southern slopes on the carbonate platform (Fig. 1, Tadaet al., 2003). The Pe~nalver Formation was deposited in onebasin located northenorthwest of the Cuban carbonate plat-form (Iturralde-Vinent, 1992, 1994, 1998).

According to the palaeogeographic reconstruction of Cubaand surrounding areas at the time of the K/T boundary impact,the proto-Caribbean basin was bounded to the north by theFlorida platform and slope deposits, to the northeast by the Ba-hamian carbonate platform and slope deposits, to the west bythe Yucatan platform and slope deposits, and to the south bythe Cuban carbonate platform (Tada et al., 2003). The basinextended southeastward to the Atlantic Ocean with a northesouth width of over five hundred kilometers (Fig. 1, Tadaet al., 2003). Between these shallow submarine platforms,continental slopes and a deep-sea basin developed witha thin oceanic crust (¼proto-Caribbean basin) in the centralpart of the proto-Caribbean sea (Tada et al., 2003). The K/Tboundary impact occurred in this palaeogeographic setting,and the K/T boundary deposits were laid down in the westernproto-Caribbean basin (Tada et al., 2003).

3. Stratigraphic setting

The latest Campanian to Eocene hemipelagic sedimentaryrocks in the Cuban foldbelt represent part of the sedimentaryinfill of basins originally located within the proto-Caribbeanbasin and above the extinct Cretaceous volcanic arc(Pszczolkowski, 1986; Iturralde-Vinent, 1992, 1994, 1998).These deposits, about 1200 m thick, have been designated inascending order as the Vıa Blanca, Pe~nalver, Apolo, Alkazar,and Capdevila formations (Bronnimann and Rigassi, 1963) orthe Mercedes Group (Albear and Iturralde-Vinent, 1985).

The Vıa Blanca Formation unconformably overlies the de-formed Cretaceous volcanic arc sequences and Mesozoicophiolite (Bronnimann and Rigassi, 1963; Albear andIturralde-Vinent, 1985). It is 500-m thick and ranges in agefrom latest Campanian to latest Maastrichtian (Tada et al.,2003). Samples from the uppermost level of the Vıa BlancaFormation in the Havana area yield latest Maastrichtian plank-tonic foraminifera (Abathomphalus mayaroensis, Plummerita

Fig. 1. Palaeogeotectonic setting of the Pe~nalver Formation in northwestern Cuba at the time of the K/T boundary impact (modified from Tada et al., 2003).

219K. Goto et al. / Cretaceous Research 29 (2008) 217e236

hantkeninoides and Pseudoguembelina hariaensis, Dıaz-Oteroet al., 2003). The formation is represented by well-beddedhemipelagic sandstones, with four or more intercalations ofgranule to pebble conglomerates. The clasts include lithics de-rived from the erosion of the extinct Cretaceous Cuban volca-nic arc, ophiolites, and limestones (Bronnimann and Rigassi,1963; Albear and Iturralde-Vinent, 1985). The depositionaldepth of the Vıa Blanca Formation in the Havana area is esti-mated as 600 to 2000 m based on the ratio between plankticand benthic foraminifera (Bronnimann and Rigassi, 1963).

The Pe~nalver Formation is 20 to >180 m thick and overliesthe Vıa Blanca Formation with an erosional contact. It is a cal-careous clastic unit at the type locality that fines upward fromcalcirudite to calcilutite and lacks bioturbation (Bronnimannand Rigassi, 1963; Takayama et al., 2000). The Pe~nalver For-mation contains various species of planktonic foraminiferafrom Campanian to late Maastrichtian age with minor Creta-ceous species younger than Aptian in age (Dıaz-Otero et al.,2000; Takayama et al., 2000). Rudist fragments, includingBarrettia monilifera and Titanosarcolites giganteus faunasthat are found in the Maastrichtian carbonate platform depositsof Central Cuba (Rojas et al., 1995), are commonly observedin the lower 30 m of the Pe~nalver Formation (Takayama et al.,2000). Takayama et al. (2000) reported the presence of Miculaprinsii from a large mudstone intraclast in the lower part of theformation, the occurrence of which is limited to the latestMaastrichtian and giving an age of between 65.4 and65.0 Ma (Bralower et al., 1995). There are no Tertiary micro-fossils in the formation. Altered vesicular glass and shocked

quartz grains of probable impact origin are found in the Pe~nal-ver Formation (Takayama et al., 2000; Goto et al., 2002;Nakano et al., in press). The biostratigraphical constraintsand occurrence of impact materials indicate that the Pe~nalverFormation was deposited subsequent to the K/T boundary bo-lide impact event (Takayama et al., 2000; Tada et al., 2003).

The overlying 100 m-thick Apolo and Mercedes formationsare not distributed around the type locality of the Pe~nalver For-mation, but a part of it is exposed at a highway junction about3 km to the southwest of the type locality of the Pe~nalver For-mation (Takayama et al., 2000, fig. 4) and Minas area (Tadaet al., 2003), approximately 4 km east from the type locality(Fig. 2). These formations are composed of hemipelagic turbi-ditic calcareous and clastic rocks (Bronnimann and Rigassi,1963; Albear and Iturralde-Vinent, 1985), and the lithologyof the Apolo Formation resembles that of the Vıa Blanca For-mation. Planktonic foraminifera within the Apolo Formationat Minas are of lower Danian age (Parvularugoglobigerina eu-gubina and Globoconusa fringa). The Apolo Formation gradesupward into chalky limestone of the Upper Paleocene toLower Eocene Alkazar Formation (Bronnimann and Rigassi,1963; Albear and Iturralde-Vinent, 1985).

4. Studied localities

The localities examined herein are situated in northwesternCuba, and extend a distance of over 150 km in an east-west di-rection. Field surveys were carried out at the type locality nearHavana, Cidra approximately 90 km to the east of Havana, and

Fig. 2. Distribution of the Pe~nalver and related formations in northwestern Cuba and studied localities (modified from Mossakovsky et al., 1988; Bronnimann and

Rigassi, 1963).


Santa Isabel approximately 60 km to the west of Havana(Fig. 2). The Pe~nalver Formation at Cidra and Santa Isabel con-tain various species of planktonic foraminifera from Campa-nian to late Maastrichtian in age (Dıaz-Otero et al., 2003).Moreover, shocked quartz grains are also reported from theselocalities (Goto et al., 2002). The mixed nature of reworkedmicrofossils, lithic fragments, and impact derived materials issimilar to the K/T boundary ‘‘cocktail’’ deposits in the Gulfof Mexico (Bralower et al., 1998), suggesting that thePe~nalver Formation in these localities were also related to theK/T boundary impact and were formed as a result of reworking.

The Havana area is situated at the western end of the east-west trending Havana-Matanzas anticline, and the Pe~nalverFormation is repeatedly exposed by folds with a wavelengthof several kilometers (Fig. 2). The Pe~nalver Formation at thetype locality is exposed in an abandoned quarry near thevillage of Pe~nalver (Fig. 2). The quarry is located on the north-ern flank of the east-west trending syncline. The Pe~nalverFormation in Cidra is exposed in an abandoned quarry locatedbetween Matanzas city and the village of Cidra, 1.5 km south-west of Santa Ana (Figs. 2 and 3). This quarry is situated in theeast-west trending Havana-Matanzas anticline. The Pe~nalverFormation in the Santa Isabel area is exposed on small hills2 km to the south of the road between the towns of Marieland Caba~nas (Figs. 2 and 3).

It is difficult to estimate palaeodepths of the Vıa BlancaFormation at Cidra and Santa Isabel using the ratio betweenplanktic and benthic foraminifers similar to the Havana area,

because the preservation of fossils in the sediments just belowthe Pe~nalver Formation in these areas is poor. On the otherhand, the Cidra and Santa Isabel areas are located approxi-mately 15 and 20 km to the south relative to the type locality,respectively, when the east-west trend folds are restored. Therestored positions of the three localities suggest that the Cidraand Santa Isabel areas were located closer to the CubanCarbonate platform, and thus their depositional depths wereprobably shallower than the type locality.

5. Analytical methods

Petrographical, mineralogical, and grain size analyses wereconducted to interpret the depositional mechanism of the Pe~nal-ver Formation. Sampling points are shown on Fig. 4. Graincomposition was quantitatively investigated by point counting.Powdered samples were analysed using X-ray powder diffrac-tion (XRD) to examine the mineral composition (Takayama etal., 2000). The siliciclastic mineral content was difficult to eval-uate for most bulk samples, because these are highly calcareous(>85%). To examine the siliciclastic minerals, 10 to 20 g ofbulk samples were treated with approximately 100 cc of 20%acetic acid for 12 h to remove calcite. Residues were thenwashed with H2O, centrifuged, and dried. Dolomite is not dis-solved by this treatment (Takayama et al., 2000). The insolubleresidues were weighed to calculate calcium carbonate content.

The maximum sizes of carbonate and detrital silicate grainswere measured under the petrographic microscope to examine

2

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Lower unit(calcirudite)

A B

Fig. 3. Route maps with sampling position in the Pe~nalver Formation around (A) Cidra and (B) Santa Isabel. Route map of the type locality is described in fig. 5 of

Takayama et al. (2000).


the grain size variation. Grain size distributions of insolubleresidues from the upper part of the Pe~nalver Formation inSanta Isabel were analyzed to examine the relationship be-tween calcium carbonate content and grain size distributionof the insoluble residue. Grain size distributions of the insolu-ble residues were determined using a Horiba LA-920 laserdiffraction grain size analyzer. The residue was treated inabout 50 cc of 0.2% aqueous solution of Na4 (P2O7) to preventcoagulation of clay particles (see Takayama et al., 2000).

6. Results

6.1. Lithology and petrology of the Pe~nalver Formation

Takayama et al. (2000) divided the Pe~nalver Formation atthe type locality into five members based on variations inlithology; Basal, Lower, Middle, Upper, and Uppermost in as-cending order (Fig. 4). They further suggested that the deposi-tional mechanism and the origin of the Basal member isdifferent from the Middle to Uppermost members based onsedimentary structures and composition. The Lower memberis interpreted as a transition between the Basal member andthe Middle to Uppermost members. Using these observations,Tada et al. (2003) defined the Basal plus lower part of theLower members into the Lower Unit, and the upper part ofthe Lower member plus Middle to Uppermost members asthe Upper Unit. The Upper Unit is subdivided into subunits

A and B, which correspond to the upper part of the Lowermember plus the Middle to Upper members, and the Upper-most member of Takayama et al. (2000), respectively (Fig. 4).In this study, the litho-stratigraphic divisions of Tada et al.(2003) are used, because their divisions are also applicablefor the Pe~nalver Formation at Cidra and Santa Isabel.

6.2. The type locality (Havana Province)

6.2.1. The Lower UnitThe sequence from the upper part of the Vıa Blanca Forma-

tion to the upper part of the Subunit A of the Pe~nalver Forma-tion is continuously exposed at the type locality (Takayamaet al., 2000, fig. 5). Subunit B of the Pe~nalver Formation isin fault contact with Subunit A and the overlying Apolo For-mation is not present at the locality.

The Lower Unit overlies the Vıa Blanca Formation with anerosional surface. It is approximately 30 m thick, and thelower 25 m consists of a light to medium gray, poorly-sorted,granule to pebble grained calcirudite (Fig. 5A). There arecommon intraclasts up to 2 m in diameter, which are probablyderived from the underlying Vıa Blanca Formation (Takayamaet al., 2000). The largest intraclast of approximately 10 m inwidth is observed in the Lower Unit of the Pe~nalver Formationin Victoria quarry (Fig. 6), which is located approximately6 km to the east of the type locality (Fig. 2). The upper 5 mof the Lower Unit consists of light to medium grey,

Fig. 4. Lithological sections of the Pe~nalver Formation and its subdivision into units and subunits. Subdivision of units by Takayama et al. (2000), and Tada et al.

(2003) and this study are also shown.


poorly-sorted, medium to coarse grained calcarenite and ischaracterized by 36 intercalations of conglomerate beds,each a few centimeters thick. The conglomerates consist ofrounded pebbles of greenish black mudstone lithics with un-common rudist fragments and shallow-marine limestonelithics. There are pillar structures in the calcarenite (Takayamaet al., 2000), similar to the stress pillars classified by Lowe(1975) as one type of fluidization channel and considered tohave been formed during settling of a dense sediment cloud(Takayama et al., 2000).

The calcirudite and calcarenite of the Lower Unit are mainlycomposed of poorly-sorted, angular to subangular, biomicritelithics (Fig. 7A) and shallow-water bioclasts dominantly com-posed of fragments of rudists (Fig. 7B), molluscs, and large cal-careous benthic foraminifera (Fig. 8). Non-carbonate grains arecomposed of poorly sorted, angular to subangular, brownishmudstone and andesite lithics, mono- and poly-crystallinedetrital quartz, and feldspar (Fig. 8). Altered vesicular glassfragments are reported in the Lower Unit and are similar inshape and texture to bubbly spherules of impact ejecta originat other K/T boundary deposits (Takayama et al., 2000).

Insoluble residue in the calcirudite is mainly composed ofquartz, smectite, clinoptilolite-heulandite and plagioclase(Fig. 9). In thin section, the quartz and plagioclase occur inthe calcirudite as individual detrital grains as well as<30 mm-sized detrital grains within the biomicrite, micriticlimestone, and mudstone lithics. Smectite is mainly in themudstone lithics, and it also partly replaces vesicular glass(Takayama et al., 2000). The maximum grain sizes of themicritic limestone lithics and detrital quartz grains show an up-ward decrease from 1240 to 720 mm and from 700 to 375 mm,respectively (Fig. 9).

6.2.2. The Upper UnitThe contact between the Lower and Upper units is grada-

tional. The top of the Lower Unit is defined as the last occur-rence of the thin conglomerate beds. The Upper Unit is morethan 150 m thick and subdivided into subunits A and B. Sub-unit A is approximately 95 m thick and its lower 55 m consistsof light to medium grey, massive, well-sorted, fine to mediumgrained calcarenite. Pillar structures are observed throughout(Fig. 5B) together with pipe structures (Fig. 5C), another

Fig. 5. (A). The calcirudite of the Lower Unit at the type locality. (B) Pillar structures in Subunit A at the type locality. (C) Pipe structures in Subunit A at the type

locality. (D) Faint parallel bedding in the upper part of Subunit A at the type locality.


type of water escape structure (Takayama et al., 2000), identi-fied within 5 beds at 18, 25, 35, 50 and 55 m above the base ofthe subunit. The pipe structures are 5e10 cm across and 20e50 cm long, and they are generally developed perpendicular tothe bedding. The upper 40 m of Subunit A consists of light tomedium gray, massive, well-sorted, very fine to fine grainedcalcarenite. In contrast to the lower 55 m of Subunit A, thereare no water escape structures. Instead, this part is character-ized by faint parallel bedding several centimeters to severalmeters thick (Fig. 5D).

Fig. 6. A large intraclast observed in the basal part of the Lower Unit of the

Pe~nalver Formation at Victoria quarry.

The calcarenite of Subunit A is mainly composed of well-sorted and well-rounded micritic limestone and crystallinecarbonate lithics, together with planktonic and benthic foramin-ifers (Figs. 7C and 8A). The content of large fossil fragments ofshallow-marine origin decreases rapidly from approximately 10to 3% at the base of Subunit A (Fig. 8A). Non-carbonate grainsare mainly composed of well-sorted, well-rounded serpentinelithics, mono-crystalline detrital quartz, and andesite lithicswith smaller amounts of feldspar, brownish mudstone lithics,and minerals such as spinel, amphibole and biotite (Fig. 8B).Serpentine lithics usually show a mesh texture (Fig. 7D), sug-gesting alteration from olivine. Serpentine lithics, which are ab-sent in the Lower Unit, appear at the base of Subunit A, rapidlyincrease upward in abundance and form approximately 50% ofnon-carbonate grains in the lower to middle part of Subunit A(Fig. 8B). The abundance of serpentine lithics gradually de-creases upward with 5 to 15 m scale variation of content in theupper part of Subunit A. As shown in Fig. 9, analysis of the abun-dance of serpentine in the insoluble residues by XRD confirmedthis observation. The insoluble residue is mainly composed ofquartz, dolomite, smectite, clinoptilolite-heulandite, plagio-clase and serpentine in the calcarenite of Subunit A (Fig. 9),with illite and siderite. The maximum grain size of micritic lime-stone lithics and detrital quartz grains in the Upper Unit showsan upward decrease from 850 to 150 mm and from 590 to100 mm, respectively (Fig. 9). Slight oscillations in maximumgrain size of micritic limestone and detrital quartz grains areobserved in Subunit A.

Subunit B is in fault contact with Subunit A with an esti-mated thickness of at least 55 m. It consists of light to medium

Fig. 7. (A). Biomicrite with planktonic and benthic foraminifers and (B) bioclast in the calcirudite of the Lower Unit at the type locality. (C) Planktonic forami-

nifera, and (D) serpentine lithics in the calcarenite of Subunit A at the type locality. (E) Calcilutite of the Subunit B at the type locality. (F) Oolite lithics in the first

calcirudite bed at Cidra. (G) Clorite-replaced opaque grain in the fifth calcirudite bed, and (H) calcilutite of the Subunit B at Santa Isabel.


grey, massive calcilutite, mainly composed of clay-sizedgrains of coccoliths, micrite and brownish clay minerals andplanktonic foraminifera (Figs. 7E and 8). The insoluble resi-due of the calcilutite is mainly composed of quartz, clinoptilo-lite-heulandite, smectite and plagioclase (Fig. 9) with siderite.Serpentine and dolomite are rare in Subunit B.

6.3. Cidra (Matanzas Province)

6.3.1. The Lower UnitThe upper part of the Vıa Blanca Formation to the upper

part of Subunit A of the Pe~nalver Formation is continuouslyexposed in an abandoned quarry near the village of Cidra.

Fig. 8. Vertical variations in grain composition of the Pe~nalver Formation at the type locality based on point counting: (A) composition of bulk samples and (B)

composition of non-carbonate grains. Legend of columnar section is same as in Fig. 4.

85 100 0 0 3000

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Fig. 9. Vertical variations in calcium carbonate content (wt %), and mineral compositions of insoluble residue based on XRD analysis (CPS), and maximum grain

sizes of carbonate and silicate grains (mm) of the Pe~nalver Formation at the type locality.



The thickness of the exposed part of the Pe~nalver Formation is85 m (Fig. 4). Subunit B and the overlying Apolo Formationare not exposed.

The Lower Unit at Cidra overlies the Vıa Blanca Formationwith an irregular erosional surface. The Lower Unit is 18 mthick and is composed of two 9 m-thick calcirudite to calcar-enite beds, defined as calcirudite beds 1 and 2 in ascendingorder (Fig. 4). The contact between the beds 1 and 2 is sharpand conformable. Each bed fines upward from pebble-grainedcalcirudite to coarse-grained calcarenite. The calciruditeshows grain-supported fabric and contains abundant well-rounded macrofossil fragments of shallow-marine origin.Thin conglomerate beds are intercalated in the upper part ofeach unit and the occurrence of these beds is similar to thatin the upper part of the Lower Unit at the type locality. Theuppermost thin conglomerate bed in Bed 2 is deformed andits upper part is cut by the overlying calcarenite of the UpperUnit. Pillar structures occur in the upper part of Bed 1 andthroughout Bed 2 (Fig. 10A).

Grain composition and size of the calcirudite and calcaren-ite of the Lower Unit at Cidra are different from that at thetype locality (Figs. 11 and 12). In Bed 1, there are numbersof well-rounded oolite lithics (Fig. 7F) and minor black shalefragments w1 mm in diameter are observed. Brownish mud-stone lithics appear different from those at the type localitybecause they contain abundant detrital quartz and plagioclase

Fig. 10. (A) Pillar structures (white streaks) in the Lower Unit at Cidra. (B) Appro

Cidra. Small amount of angular black shale fragments are observed. (C) The irregu

of grey and hard calcilutite bed and light grey and more calcareous bed in Subun

grains with diameters less than 50 mm. Moreover, the maxi-mum size of micritic limestone lithics in the Lower Unit atCidra is coarser than those at the type locality, and show up-ward decrease from 2300 to 1700 mm (Fig. 12). The insolubleresidue of the calcirudite in the Lower Unit is similar in com-position to that at the type locality, although the content ofclinoptilolite-heulandite in Cidra is slightly higher than thatat the type locality (Fig. 12).

6.3.2. The Upper UnitSubunit A of the Upper Unit overlies the Lower Unit with

an irregular erosional surface. It is more than 67 m thick andcomposed of light grey, massive, well-sorted, medium to finegrained calcarenite. Pillar structures are observed throughout,although pipe structures occur at only two distinct levels, 1and 20 m above the base of the subunit (Fig. 4). There is anapproximately 1 m-thick interval with faint parallel laminationfrom 27 to 28 m above the base of this subunit. This interval isassociated with a small amount of angular black shale frag-ments up to 20 cm in diameter (Fig. 10B), which tend to bealigned parallel to bedding. Above this interval, several centi-meters to several meter-thick faint bedding is observed.

Grain composition and size of the calcarenite in Subunit Ais similar to that at the type locality (Figs. 11 and 12). Thecontent of shallow marine large fossils drastically decreaseswithin the lower part of Subunit A. Serpentine lithics are not

ximately 1 m thick interval at 27 to 28 m above the base of the Subunit A at

lar contact between the Lower and Upper units at Santa Isabel. (D) Alternation

it B at Santa Isabel.

Fig. 11. Vertical variations in grain composition at Cidra.


found in the Lower Unit, but appear at 10 m above the base ofSubunit A, where the content of large fossil fragment of shal-low marine origin and biomicrite lithics decrease (Fig. 11).Serpentine lithics comprise more than 50% of non-carbonategrains between 10 and 27 m above the base of Subunit Aand decrease upward with oscillations of their content between

10070

Low

erun

it

The

Peñ

alve

r Fo

rmat

ion

Upp

er u

nit

Subu

nit A

200 0 3000

0m

50

85


Dolomite(CPS)

Serpentine(CPS)

0

Fig. 12. Vertical variations in calcium carbonate content (weight %), and mineral co

and silicate grains (mm) at Cidra.

0 and 50% (Fig. 11). Brownish mudstone lithics in Subunit Ado not contain detrital quartz and plagioclase grains, indicatingthat mudstone lithics differ between the Lower and Upperunits. The range of maximum grain size and upward decreas-ing trend of both micritic limestone lithics and detrital quartzgrains in Subunit A at Cidra are almost the same as those at the

0.1 1

0

10

0 600

0 3000 0 1000

3000

Quartz(CPS)


Smectite(CPS)


Plagioclase(CPS)

mpositions of insoluble residue (CPS), and maximum grain sizes of carbonate


type locality (Fig. 12). Insoluble residue in the calcarenite ofSubunit A is similar to that at the type locality, including anupward increasing trend of quartz and clinoptilolite-heuland-ite, upward decreasing trend of smectite, and presence of ser-pentine only in Subunit A (Fig. 12).

6.4. Santa Isabel (Pinar del Rio Province)

6.4.1. The Lower UnitThe interval from the upper part of the Vıa Blanca Forma-

tion to the lower part of the probable Apolo Formation is con-tinuously exposed at Santa Isabel. The thickness of thePe~nalver Formation in this area is approximately 80 m(Fig. 4).

The Lower Unit of the Pe~nalver Formation overlies the VıaBlanca Formation with an irregular erosional surface. Thethickness of the Lower Unit is 45 m and is composed of fiveamalgamated calcirudite beds, which are defined as Beds 1to 5 in ascending order (Fig. 4). Each bed shows upward-finingfrom cobble-grained calcirudite to coarse-grained calcarenite.The calcirudite shows a grain-supported fabric and containsabundant well-rounded macrofossil fragments of shallow-marine origin. Abundant intraclasts up to 2 m in diameterare entrained in Bed 1. Thin conglomerate beds are interca-lated in the upper part of beds 1, 4 and 5, and these are similarto those observed in the upper part of the Lower Unit at thetype locality and Cidra. Channel-type erosional surfaces areobserved in the basal parts of beds 2, 4 and 5. Axes of theseerosional channel surfaces trend in a NeS direction andplunge 3� to the north with respect to bedding.

Fig. 13. Vertical variations in grain

Grain composition and size of the calcirudite of the LowerUnit at Santa Isabel is different from that at the type localityand Cidra (Fig. 13). Large calcareous benthic foraminiferaare not observed in Bed 1. Brownish mudstone lithics are dif-ferent from those at the type locality, but similar to those atCidra in that they contain abundant detrital quartz and plagio-clase less than 50 mm in diameter. There is no significantcompositional variation between beds 1 to 4, whereas chlo-rite-replaced grains are observed in Bed 5 (Fig. 7G). Theinsoluble residue of the calcirudite in the Lower Unit is similarin composition to that at the type locality (Fig. 14). In Bed 5,quartz is more and smectite less abundant than in beds 1 to 4,and chlorite and minor dolomite are present. The maximumsize of micritic limestone lithics in the Lower Unit at SantaIsabel is coarser than those at the type locality and Cidra,and show an upward decrease in size from 7300 to 1300 mm(Fig. 14).

6.4.2. The Upper UnitThe Upper Unit overlies the Lower Unit with an irregular

erosional surface (Fig. 10C). The Upper Unit is approximately35 m thick and subdivided into subunits A and B. Subunit A is8 m thick and consists of medium grey, massive, well-sorted,very fine to fine grained calcarenite. The lower 2 m of SubunitA is composed of an alternation of fine and very fine calcaren-ite. An approximately 1.6 m deep channel-type erosional sur-face is observed 2 m above the base of Subunit A. The channelaxis trends approximately N77�W and plunges 10� to the westrelative to bedding. No water escape structures are observed inSubunit A. Grain composition and mineral composition of

composition at Santa Isabel.

0 100.01

0m

50

Peña

lver

For

mat

ion

Upp

er u

nit

Low

er u

nit

Sub

A

Subu

nit B

3000 0 1000 185 10070


Dolomite(CPS)

Quartz(CPS)

Smectite(CPS)


Chlorite (CPS)

2000 3000


Plagioclase(CPS)

00 600 3000

0

Fig. 14. Vertical variations in calcium carbonate content (wt %), and mineral compositions of insoluble residue (CPS), and maximum grain sizes of carbonate and

silicate grains (mm) at Santa Isabel.


insoluble residues of the calcarenite is similar to that at theupper part of Subunit A of the type locality and Cidra, exceptfor the absence of serpentine lithics and dolomite (Figs. 13 and14). The range of maximum grain size and upward decreasinggrain size trend of both micritic limestone lithics and detritalquartz grains in Subunit A are similar to those at the typelocality and at Cidra (Fig. 14).

Subunit B overlies Subunit A with a sharp conformable con-tact. It is approximately 27 m thick and is characterized by tenalternations of grey argillaceous calcilutite beds 1 to 4 m thickand light-grey calcilutite beds several to several tens centimeterthick (Figs. 10D and 15). The carbonate content of light-graycalcilutite beds is 3 to 8% higher than the grey argillaceous cal-cilutite beds (Fig. 15). The grain-size distribution of insolubleresidue in the calcilutite shows an uni-modal distribution(Fig. 16). The average mode and maximum diameters of the in-soluble residue of the light-grey calcilutite beds are approxi-mately 5.1 and 20 mm, whereas those of the grey argillaceouscalcilutite beds are approximately 5.9 and 45 mm, respectively.Furthermore, the grey argillaceous calcilutite beds have broadergrain-size distributions than those of the light-grey calcilutitebeds. The calcilutite in Subunit B is mainly composed ofclay-sized grains such as coccolith and micrite matrix withsmall amount of well preserved planktonic foraminifera (Figs.7H and 13); secondary calcite is rare. The light-grey calcilutitebeds contain a larger amount of micritic limestone lithics andplanktonic foraminifera than the grey argillaceous calcilutite

beds. The contents of coccolith and micrite matrix are alsohigher in the light-grey calcilutite beds. On the other hand,the grey argillaceous calcilutite beds contain more detritalquartz and andesite lithics than the light-grey calcilutite beds.

At the top of the Subunit B, there is a 2 to 7 cm thick browncalcilutite bed with burrows. An iridium concentration anom-aly (179� 30 ppt) is observed in this bed, and slightly de-creases to 91� 16 ppt just above the bed (Hatsukawa et al.,2007). These values are well above the background level(<47 ppt, Hatsukawa et al., 2007), but low when comparedwith other K/T boundary deposits around the proto-Caribbeansea and the Gulf of Mexico (e.g., Smit et al., 1992). Above thisbed, there is a 4 m thick light-grey massive calcilutite inter-preted as the Apolo Formation.

7. Discussion

7.1. Lateral variation in lithology of the Pe~nalverFormation

The results of this study indicate that the thickness and sed-imentary structures of the Pe~nalver Formation show significantand systematic lateral variations. The Pe~nalver Formation ismore than 180 m thick at the type locality, more than 85 mat Cidra, and approximately 80 m at Santa Isabel (Fig. 4 andTable 1). Notably, at Santa Isabel and Cidra, the Lower Unitcomprise a larger number of calcirudite beds, contains a larger

Subu

nit B

55m

60

65

70

75

80

Sub A 80 85calcium carbonate content (wt )

Apo

lo F

m.

90

Fig. 15. Vertical variation in calcium carbonate content (wt %) in the Subunit

B at Santa Isabel.

0

4

8

12

0.1 1 10 100

Grain size ( m)

Vol

ume

()

light-gray calcilutite (average of 11 samples)

gray argillaceous calcilutite(average of 21 samples)

Fig. 16. Grain size distributions of insoluble residues of the Subunit B at Santa

Isabel (mm).

Table 1

Lateral variations of thickness and sedimentary features of the Penalver

Formation

Type locality Cidra Santa Isabel

Total thickness >180 m >85 m 80 m

Depositional area Offshore Near the arc Near the arc

Lower unit

Thickness 30 m 18 m 45 m

Number of

calcirudite beds

1 2 5

Relative

depositional depth

Deep Shallow Shallow

Upper unit

Thickness >150 m >67 m 35 m

Basal contact Gradual Weakly eroded Strongly eroded

Current structure No Yes Yes

Compositional

oscillation

Subunit A Subunit A Subunit B

Number of

oscillation

>6 >7 10


amount of biomicrites and shallow marine fossil fragments,and is coarser grained than at the type locality (Table 1).This suggests that the Pe~nalver Formation at Cidra and SantaIsabel were deposited at shallower depths and closer to thesource area than at the type locality. This is consistent withthe finding that, of the three localities, the type locality was lo-cated northward and furthest away from the Cuban carbonateplatform when restored to its original position.

7.2. Origin and depositional mechanism of the LowerUnit

The Lower Unit of the Pe~nalver Formation overlies the VıaBlanca Formation with an irregular erosional basal contact,and entrains calcareous mudstone blocks of the Vıa BlancaFormation as intraclasts at all localities studied. The calciru-dite in the Lower Unit is poorly sorted with a grain-supportedfabric, and is composed of abundant well-rounded macrofossilfragments of shallow-marine origin. It includes pillar typewater escape structures at both the type locality and Cidra.All these features in the Lower Unit are consistent with thoseof debris flow deposits (Middleton and Hampton, 1976).

Dypvik and Jansa (2003) mentioned that the Pe~nalver For-mation was derived not from the Cuban volcanic arc but froma continental margin due to the collapse of the outer shelfedge, based on the presence of quartz and microcline grains.However, these grains are also observed in the sediments ofthe Vıa Blanca Formation and have not necessarily been


transported from a continental margin. Moreover, the rudisttaxa (Rojas et al., 1995), the presence of andesite lithics inthe Lower Unit, and NeS direction of channels developed inthe basal part of beds 2, 4 and 5 at Santa Isabel suggest thatthe calcirudite of the Lower Unit was derived from the extinctCretaceous Cuban arc exposed to the south of the depositionalarea of the Pe~nalver Formation and from the underlying con-glomeratic beds of the Vıa Blanca Formation, as previouslyproposed by Takayama et al. (2000). Well-rounded oolite frag-ments are only observed in Bed 1 at Cidra and chlorite-replaced grains are observed only in Bed 5 at Santa Isabel.Furthermore, the maximum grain size of carbonate and silicategrains in each bed in the Lower Unit is different. Differencesin grain and mineral composition, and maximum grain size ofcarbonate and silicate grains in the calcirudite of the LowerUnit among the studied localities suggest a local source forthe debris flows.

According to Goto et al. (2002), there are no shockedquartz grains in the calcirudite Bed 1 at Cidra and in beds 1to 3 at Santa Isabel. Because shocked quartz grains probablysettled around the impact site within several hours after the im-pact (Kring and Durda, 2002; Tada et al., 2003), the debrisflows, which led the deposition of these beds, were generatedand deposited within several hours after the impact before thearrival of shocked quartz grains to the sea floor. One of the ear-liest impact-related phenomena arriving at the sites are theseismic waves (e.g. Smit et al., 1996; Smit, 1999), whichmay have arrived at the studied area within several minutes af-ter the impact. Their effect continued for several hours, andpeak amplitude of the seismic waves could have reached sev-eral meters (Boslough et al., 1996), enough to cause largeslope failures (Takayama et al., 2000; Tada et al., 2003). Alter-natively, large-scale tsunami created by large-scale slope fail-ure along the Yucatan platform margin may have served astriggers of debris flows (Tada et al., 2003). Since the distancebetween the Yucatan platform margin and the depositionalarea of the Pe~nalver Formation was approximately 400 km,the first tsunami could have arrived at the depositional area ap-proximately 1 h after slope failure (Matsui et al., 2002).

7.3. Origin of the Upper Unit

Fig. 17. Serpentine lithics in the serpentine sandstone at Moa area.

In the Upper Unit of the Pe~nalver Formation, hemipelagicgrains such as micritic limestone lithics and planktic and ben-thic forams are major components of the calcarenite, suggest-ing a distinct difference in the source compared to the LowerUnit. Planktonic foraminiferal assemblages in the Upper Unitat the type locality are characterized by a mix of various spe-cies with various diagnostic ages ranging from Campanian toMaastrichtian (Takayama et al., 2000), which overlap with theage of the Vıa Blanca Formation. Similar micritic limestonelithics and skeletons of planktic and benthic forams are abun-dant in turbidites in the Vıa Blanca Formation, suggesting thatthe major source of the Upper Unit was unconsolidated sedi-ment of the Vıa Blanca Formation on the slope of the Cubancarbonate platform rather than the actual carbonate platformsediments. This is postulated because there are no carbonate

lithics derived from the carbonate platform in Subunit A atthe type locality. Debris flows, which led to deposition ofthe Lower Unit, may have contributed to resuspension of theunconsolidated sediments of the Vıa Blanca Formation, be-cause debris flows usually erode and entrain sediments downslope (Postma et al., 1988). However, the presence of serpen-tine lithics, which occupy less than 50% of total non-carbonategrains, and nannofossils and planktonic foraminifera of Aptianage in the Upper Unit are difficult to explain simply by resus-pension of sediments from the Vıa Blanca Formation by debrisflows, because these are not present in the Vıa Blanca Forma-tion in the study area.

Although there is no serpentinite and serpentine sandstonebeds in the Vıa Blanca Formation, serpentinite and relatedrocks are present in sections beneath the Vıa Blanca Formationin the Havana area and a small amount of serpentine pebbles ofthe same origin are observed in the Lower Unit of the Pe~nalverFormation in Victoria. However, these serpentinite exposuresand serpentine pebbles have grain sizes very differentfrom sand-size serpentine lithics in the Upper Unit. On theother hand, Maastrichtian serpentine-rich sandstones andconglomerates, related to allochthonous ophiolites bodies, areexposed in central to northeastern Cuba. For example, Maas-trichtian serpentine-rich sandstones at south of Moa approxi-mately 500 km to the east of Havana (La Picota Formation,Mossakovsky et al., 1988) are composed of well-sorted, suban-gular to rounded, fine to medium grained serpentine grains. An-other possible source is Loma Capiro, central Cuba, because atthis locality there are calcarenites with serpentine lithics ofMaastrichtian age. The grain size distribution and roundnessof these serpentine grains are similar to serpentine lithics inthe Upper Unit of the Pe~nalver Formation (Figs. 17 and 18).Such similarities suggest that serpentine sandstone in centralto northeastern Cuba could be the source of serpentine lithicsin the Upper Unit at the type locality and Cidra.

There are no serpentine lithics in the Upper Unit at SantaIsabel. However, medium to coarse grained calcarenite is ab-sent in the Upper Unit at Santa Isabel. Serpentine lithics areabundant in medium to coarse grained calcarenites in thelower to the upper part of Subunit A at the type locality and

0

10

20

30

40

0 120 240 360 480

Fre

quen

cy (

)F

requ

ency

()

Peñalver Formation(type locality)

0

10

20

30

40

0 120 240 360 480

Moa

A

B

grain size ( m)

grain size ( m)

Fig. 18. Grain size distributions of serpentine lithics (mm) in (A) Subunit A at

the type locality, and (B) Cretaceous serpentine sandstone at Moa area based

on thin section observation.


Cidra, but they are rare in very fine to fine calcarenite in theuppermost part of Subunit A at the type locality (Fig. 9). Con-sequently, the absence of serpentine lithics in Santa Isabelcould be explained by absence of the medium to coarsegrained calcarenite at the base of Subunit A at Santa Isabel.The presence of an erosional surface at the base of SubunitA suggests that medium to coarse sized calcarenite with ser-pentine lithics were not deposited but carried downslope aswill be discussed in the next section. Alternatively, serpentinelithics may not have reached this area, because either this areawas located in the western side of the basin or was at shallowerdepths compared to the other two localities.

7.4. Depositional mechanism of the Upper Unit

The large thickness, presence of abundant water escapestructures and finer grain size with monotonous upward finingfeature of the Upper Unit compared with that of the LowerUnit together with its homogeneous appearance with no bio-turbation at the type locality implies rapid sedimentationfrom a dense sediment suspended cloud (Takayama et al.,2000). Grain and mineral composition and maximum grainsizes of the micritic limestone lithics and detrital quartz grainsof the calcarenite and calcilutite in the Upper Unit are similarat the 3 localities, suggesting that the Upper Unit was formedfrom a homogeneous dense sediment suspension cloud at least150 km wide in an east-west direction and 20 km wide ina northesouth direction. This feature is similar to that of theSantorini-generated homogenite and implies that the densesediment suspension cloud was generated by tsunami(Takayama et al., 2000). Subunit A of the Upper Unit containsserpentine lithics that are not contained in the underlying VıaBlanca Formation, but similar to those reported from central tonortheastern Cuba. Moreover, there is no erosional surface atthe base of the Upper Unit at the type locality. These

observations suggest that serpentine lithics may have beentransported not by sediment gravity flow but as suspensiongenerated by mass water motion. This, in turn, suggests thatsediment particles may have been transported by tsunami be-cause usual marine currents cannot transport thick clouds ofsediment particles (e.g. Kastens and Cita, 1981).

The occurrence of K/T-boundary tsunami deposits in thedeep-sea has been suspected with the main argument that im-pact-generated tsunamis cannot affect the deep-sea bottom,due to the diminishing power of currents with increasing waterdepth (e.g., Bohor, 1996). However, according to the small-amplitude water wave theory (e.g., Horikawa, 1978), the influ-ence of a tsunami does not diminish downwards. This suggeststhat sediment particles on the ocean bottom have the potentialto become suspended by passing tsunami waves (Dypvik andJansa, 2003), depending on their wave height and period.

Examination of the lateral lithological variation of the Up-per Unit revealed that it is thinner at Santa Isabel and Cidra(Fig. 4 and Table 1). At these two localities, an erosionalsurface is recognized at the base and parallel lamination wasrecognized in the middle part of the Upper Unit (Table 1). Achannel-type erosional surface is observed 2 m above thebase of Subunit A at Santa Isabel, which has an axial directiondifferent from those observed in the basal part of beds 2, 4 and5 of the the Lower Unit. This probably suggests that the ero-sional surface in Subunit A was created by a process differentfrom that in the Lower Unit. Considering that depositionaldepths in the Cidra and Santa Isabel area could have been shal-lower than that of the type locality, the presence of erosionalsurfaces and parallel lamination in these areas probably re-flects the larger near-bottom current velocities of tsunamidue to the shallower depositional depths, because the near-bottom current velocity of the tsunami becomes larger withdecreasing depositional depth.

7.5. Compositional oscillations in the Upper Unit

Analysis of grain and mineral compositions of the insolubleresidue in Subunit A at the type locality reveals more than 6repeated oscillations in serpentine content (Figs. 8 and 9). Ser-pentine lithics, which were probably derived from central tonortheastern Cuba, were mixed with sediment particles resus-pended from the Vıa Blanca Formation and unconsolidatedsediments on the Cuban platform, probably by the first tsu-nami wave to form a sediment suspension cloud. This is basedon the observation that serpentine lithics appear and markedlyincrease upward from the base of Subunit A. Based on thegrain composition analysis, serpentine content is negativelycorrelated with contents of andesite and micritic limestonelithics (Fig. 8). Moreover, higher contents of micritic lime-stone and andesite lithics tend to coincide with the coarsermaximum size of micritic limestone lithics, suggesting that os-cillations in serpentine content could reflect variation of themixing ratio between two end-members characterized by ser-pentine lithics with smaller grain sizes, and micritic limestoneplus andesite lithics with larger grain sizes, respectively. Thiscan be explained by sediment particles, including coarser


micritic limestone and andesite lithics derived from the slopeof the extinct Cretaceous Cuban arc, being repeatedly injectedinto an initial dense sediment suspension cloud characterizedby serpentine lithics. Since there are no erosional structuresat the bottom of the intervals where micritic limestone and an-desite lithic contents increase, the lateral supplies of the sedi-ment particles characterized by serpentine lithics to the initialdense sediment suspended cloud should not have been in theform of gravity flows running down on the ocean floor butrather as lateral injection of the suspended particles into thesuspended cloud by northward water mass movement suchas repeated tsunami backwashes (Fig. 19).

The calcilutite of Subunit B at the type locality is massiveand without any sedimentary structures, suggesting that the in-fluence of tsunami at the type locality ceased before depositionof Subunit B and the suspended sediment particles settled mo-notonously through the ocean column (Fig. 19). In contrast, 10repeated compositional oscillations, characterized by varia-tions in calcium carbonate content, are observed in SubunitB at Santa Isabel. The grey argillaceous calcilutite beds arecharacterized by coarser grain size of insoluble residues,higher amounts of detrital quartz and andesite lithics, andlower contents of planktonic foraminifers and micritic lime-stone lithics as compared to light-grey calcilutite beds. Thissuggests that oscillations in calcium carbonate content indicatevariations of the mixing ratio between two end-members char-acterized by a higher content of carbonate grains such asplanktonic foraminifers and micritic limestone lithics withsmaller grain sizes, and a higher content of detrital quartzand andesite lithics with larger grain sizes, respectively. Thissuggests that, compared to the light grey calcilutite beds, the

Fig. 19. A cartoon showing the depositional processes of the Pe~nalver Formation. (

wave and backwash associated with the impact eroded the deep sea floor and forme

slope sediments and backwashes of tsunami transported the sediments into the dens

settled down.

grey argillaceous calcirudite beds contain larger amount ofsediment particles transported from the area of the extinctCretaceous Cuban arc. By analogy with the depositionalmechanism of Subunit A at the type locality and Cidra, com-positional oscillations in Subunit B at Santa Isabel is consid-ered to reflect repeated injection of the sediment particlesderived from the Cretaceous Cuban arc characterized by lowercalcium carbonate content and larger grain sizes into the densesediment suspended cloud characterized by higher content ofcalcium carbonate particles and smaller grain sizes as a resultof repeated tsunami backwashes.

Compositional oscillation is observed in Subunit A at thetype locality and Cidra, whereas it is observed in Subunit Bat Santa Isabel. It is possible that compositional oscillationsin Subunit B at Santa Isabel were formed by the same tsunamiwhich formed the oscillations in Subunit A at the type localityand Cidra, because the Pe~nalver Formation at Santa Isabel wasprobably deposited in shallower depth than at the type localityand it is consequently the silt size grains in the Subunit B atSanta Isabel were settled earlier than those in Subunit B atthe type locality. Our preliminary calculation suggests that os-cillations in Subunit A at the type locality and those in SubunitB at Santa Isabel could have been formed around the sametime (Goto et al., 2002).

7.6. Lithological and compositional similarities of K/Tboundary deposits in the proto-Caribbean sea and theGulf of Mexico

There is a similarity between the lithology and compositionof the K/T boundary deep-sea tsunami deposits in the Upper

A) The impact seismic wave triggered the debris flows, (B) first large tsunami

d the dense sediment suspended cloud, (C) following tsunami waves eroded the

e sediment suspended cloud, and (D) re-suspended silt size sediment particles


Unit of the Pe~nalver Formation, and the 450 m thick calcaren-ite and calcilutite part of the Cacarajıcara Formation in Cuba(Tada et al., 2003), corresponding to the Middle Grainstoneplus Upper Lime Mudstone members of Kiyokawa et al.(2002). Notably, the depositional areas of the Pe~nalver andthe Cacarajıcara formations were 400e500 km apart at thetime of the impact (Fig. 1). Moreover, Alegret et al. (2005)also inferred a similarity in lithology and composition of be-tween 4.5-m thick calcarenite and calcilutite parts of the K/T boundary deposit at Loma Capiro with the Upper Unit ofthe Pe~nalver Formation. The deposit at Loma Capiro isapproximately 10 m thick and was formed along the Cubanvolcanic arc approximately 250 km apart from the Havanaarea (Fig. 1). These similarities in lithology and compositionprobably suggest that a sediment suspended cloud of moreor less the same composition was formed and spread through-out the basin of the proto-Caribbean sea at least along theYucatan and Cuban carbonate platforms.

In addition, the approximately w350-m-thick late Maas-trichtian Amaro Formation, which was formed on the BahamaPlatform (Fig. 1, Iturralde-Vinent, 1992), is reported as thepossible K/T boundary deposits (Pszczolkowski, 1986; Itur-ralde-Vinent, 1992; Tada et al., 2003). Although its K/Tboundary impact origin has not been confirmed, it is specu-lated as the K/T boundary deposits based on the similarityin lithology and composition with the Pe~nalver Formation(Tada et al., 2003). If the Amaro Formation was formed in as-sociation with the K/T boundary impact, a sediment suspendedcloud might have been formed and spread throughout the basinof the proto-Caribbean and resulted in deposition of the thick,homogeneous, sandy to silty single-graded sediments, so-called ‘‘homogenite unit (Tada et al., 2003)’’, throughout thedeeper part of the proto-Caribbean basin.

On the other hand, the calcarenite and calcilutite parts ofthe K/T boundary deep-sea deposits at DSDP sites 536 and540, which are located on a submarine ridge along the baseof the Campeche and Florida escarpments (Fig. 1), have grainand mineral compositions (Alvarez et al., 1992) different fromthose of the Upper Unit of the Pe~nalver Formation. The differ-ence in composition between the Upper Unit of the Pe~nalverFormation and the calcarenite and calcilutite parts at theDSDP sites suggests that sediment suspended cloud was het-erogeneous at a larger scale.

In the Atlantic Ocean, only millimeter-thick to centimeter-thick distal ejecta layers have been found (e.g., Norris andFirth, 2002) and there seems to be no distinct K/T boundarytsunami deposit. This suggests that the effect of the tsunamiwas restricted within the proto-Caribbean sea and the Gulfof Mexico regions. At the time of the K/T-boundary impact,the impact site was surrounded by land in the north andwest, and shallow carbonate platforms existed in the southand east (Tada et al., 2003). Therefore, the energy of the tsu-nami might have been trapped in the Gulf of Mexico and theproto-Caribbean regions (Dypvik and Jansa, 2003).

The Pe~nalver Formation is characterized by the >6e10compositional and grain size oscillations that probably reflectsthe repeated tsunamis. Similar numbers of repetitions of

tsunami are inferred from the K/T boundary deposits charac-terized by repeated bi-directional cross laminations at La La-jilla in the coastal region of the Gulf of Mexico, whichrepeated more than 9 times (Smit et al., 1996). Furthermore,Tada et al. (2002) reported that the Moncada Formation ineastern Cuba has ripple cross-laminations at several levelsthat indicate northesouth trending palaeocurrent directionswith reversals (Tada et al., 2002). Tada et al. (2002) inferredthat the Moncada Formation was formed by repeated tsunamibased on repetition of upward fining units, reversing currentdirections between the units, systematic upward decreases inunit thickness, and an absence of basal erosional surfaces.They also reported grain size oscillations in detrital quartzgrains that repeated more than 10 times and were interpretedas representing the influence of currents (Tada et al., 2002).This agreement in number of tsunami around the impact sitesuggests that sedimentation of the Pe~nalver Formation couldhave been caused by the same tsunami waves that causedthe sedimentation of these K/T boundary tsunami deposits.

8. Conclusion

Lateral lithological, compositional and grain size variationsof the Pe~nalver Formation were examined to evaluate thedepositional mechanism. The Lower Unit of the Pe~nalver For-mation is a debris flow deposit derived from the carbonateplatform developed on the extinct Cretaceous Cuban arctogether with the Vıa Blanca Formation deposited on theslope. The Upper Unit was deposited from the dense sedimentsuspended cloud generated by the impact-induced tsunami.The regional homogeneity of source materials of pelagic tohemipelagic origin and presence of allochtonous materialssuch as serpentine lithics support the interpretation that theUpper Unit was formed by tsunami. Examination of the laterallithological variations revealed that the thickness and sedimen-tary structures of the Pe~nalver Formation change systemati-cally with changing depositional depth, which probablyreflects the difference of influence of tsunami. The sedimentson the slope of the extinct Cretaceous Cuban arc were repeat-edly eroded by tsunami and transported by backwashes intothe initial dense sediment suspended cloud, which causedcompositional oscillations in Subunit A at the type localityand Cidra and in Subunit B at Santa Isabel.

Acknowledgements

This research was made possible thanks to an agreementbetween the Department of Earth and Planetary Science, theUniversity of Tokyo and the Museo Nacional de HistoriaNatural (Agencia del Medio Ambiente) and the Instituto deGeologıa y Paleontologıa del Ministerio de Industria Basicade Cuba. We wish to thank specially the important supportprovided to field research in Cuba by Mitsui & Co., Ltd. aswell as the manager A. Nakata in Havana. We also thank G.Price, D. Tappin and P. Schulte for their critically reading ofthe manuscript and giving many valuable suggestions, andH. Takayama for his participation in the early stage of this


project. The study was supported by Grant-in-Aid for JapanSociety for the Promotion of Science (JSPS) provided to T.Matsui (no. 17403005) and research funds donated to theUniversity of Tokyo by NEC Corp., I. Ohkawa, T. Yoda, K.Ihara, and M. Iizuka, and the above mentioned institutionsin Cuba.

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