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A Model for the Early Evolution of the Gulf of Mexico Basin

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A Model for the Early Evolution of the Gulf of Mexico Basin ________________________________________o~C~ E=A~N~O~L~O~G~'~C~A_A~C~T_A~. _, _98~,~. _N_.~S~P_1~-------- Gulf of Mc:o:lco Seismic data Rifling phase Subsidence A model for the early evolution Drif! Golfe du Me"iqu(' Données sismiques r hase de di s ( en~ion Subsidence of the Gulf of Mexico basin W placcmenl R. T . Buffler ". F. J. Shaub ", R. Huerta ' , A. Il . K. Ibrahim ", J . S. Walkins ~ • Universit y of Te'las Marine Science InstiWle. 700 The Strand , Galveston . Te:< ••5 77550. USA. b Gulf Science and Technology Company. Explonttion llnd Production Di vision , 1'.0 . 80x 20]8, Pinsburgh. Pennsylvania 15230. USA. ABSTRAC T Seismic rdlcelion and refraC lio" data from the deep Gulf of Mexico basin conslrain the early geologic evolution o f the b<tsin . Ma jor observations involving distributio n of the crust. nature and d islribution of the carly sediments, and subsidence history are as foll ows ; 1) inferred oceanic crust in the deep central Gulf (5 to 6 km thick : 6JI to 7. 1 km/sec.) is rl ankcd symmctriçally on the nOrl h and south by inferred transitional crust (8 to 15 km thick ; 6.4 to 6.8 kmfsec.); 2) acollstic basement seen on the rdleçtion d,lia in the central Gulf is an irregul ar rcf[cctor and probably represent s the top of an oceanic vo1ca nic (basal tic) layer (layer 2) ; 3) north of the: Campeche Escarpmcnt thc top of transitÎonal crust is represented by a strong. smooth reflectorfunconformity that truncates rift bllsins and is onlappcd by a thick salt and sedimentary sectio n ; 4) in the southeastern Gulf transitional crust consists of tilted basement blocks probably represe nti ng a thinned and rifted conti nental crust ; lows between the blocks are filled with synrift sediments; 5) thi ck salt symmetricall y fl anks the nonh and south sides of the oceanic crust : 6) seismic stratigraphie anal ysis suggests thll t early sediments in the Gulf in areas o f transi tional crust represent an upward gradation from volcanics ,tnd nonmarine sediments induding ev.. porilcs to shallow marine and then to deep marine ; o nl y deep marine sediments OCCll r in the central Gulf overl ying oceanic crust. These data suggesl the following evolulionary sequence. The early Gulf of Mellico basin evolved as a di ve rgent (passive) continental margin at the same time and by the same mechaniSmS a!> the North-A tl antic m:;rgin. induding the formation of ncw occanic crust. We specul ate that a rifl p/rase during the Triassic-Juntssic was accompanied by widespread doming. rifting. and filling of rift basins with vo1ca nics and nonmarine rocks as North America began separating from Afri ca-South Ameri ca. Formation o f the thi nned transitio nal crust occurred dudng thi s peri od. During the latter P,t Tl o f this phase (Middle-Lule J unlssic) the Gulf area hro ke up into a series of separate subsidi ng basins; in sorne o f thcsc basins thick S;tlt WltS depositcd in shaltow marine environments. A drifl lInd .J/lbside'lee pill/se began in Late Jurassic lime (approximalely 150 my B. P.) with major rifting of the central Gulf and formation of new ocean crust. The Yuclllan block probably mOI/cd awa )' from North America ,llo ng NW·SE trcnding flow lines parullel to the North-A tl antic fracture z.o nes. separating the salt basin on eit her side o f the new crust. Spreading apP;irently was brie!. but the basin continued to subside rapidl y due to thermal çooling of the lithosphere. Subsidence was accompanicd by gnlVi ty flowage of salt in to the basin and Ihc extensive buildup of carbon[l\ e margins along a teclonic hinge zone near the periphery of the basin. Shallow- to decp-w;ttcr sediments were depositcd .. Jong the margins of the basin , while o nl y deep-water sediments were deposited in the ncwly- formed ocean basin. The carl y cvolulio n of thc basin cnded with a major middre Cret,tceous cvent that produced ,1prom inenl G urf-wid!! unconformilY. Total subsidence o f the basin since formation of the ocean crust has been up 10 10 km. partly due 10 sedimentloading and partly duc to cooling of Ihe lithosphere. Oeel/lloi. Acw. 1981. '>roceedings 26, h International Geologklll Congre!> s. Gcolog )' of continental margins symposium . Paris. luly 7- 17. 19HO. 129-136. 129 A T. BUFFlER el si. RESUME Modèle de révolution initiale du bassin du Golfe du Mexique Les données do: si~ mique réneClion el réfraclion du bassin profond du GoJf~ du ~fcxique fourni~senl des guides pour le modèle d 'évolmion géologique initiale du bassin. Le ~ princi palcs observatio ns. incluant ];1 géométrie dc la croûte. la nature el la répartition de ~ sédiments inil iaux sont les suivanlelo: 1) la crOÛ le océanique supposée dans la partie cenlmle profonde du Golfe (5 à 6 km d·épai ~~c ur : 6.8 à 7,1 kl1tls) est bordée ~ymét riq ucmcn t au Nord el au Sud par unc croûle supposée de transition (8 à 15 km d ·épai~~eur : 6.4 à 6.8 kmfs) : 21 le substratum acousliquc visible sur les données de s i ~ miquc réflection dans le Gol(e eenlral eSI un réflecteur irrégul ier représenwnt probable ment le toit d·un niveau volcanique (basaltique) correspondant à la couche 2 : 3) au nord de rescarpcmenl de Campêche. le toil de la croûle tran~ilionnelle est représenté par un fort réflecteurldilocontinuilé régulier qui limite le~ bassins du rift ct cst surmonté Ù·llne é pai s~e couche de sel et de sédiments: 4) dan~ Ic Gol fe méridional. la crOU le de Iran'i ilion csl constituée de blocs de substratum basculé~ corrcspon­ dant probilble ment li une croûte continenlale amincie et effondrée: Ic s crcux enlre les blocs sont comblés par le s sédiments ~y n - rift : 5) rhorizon salifèrc borde symétriquement le~ cx trémités nord CI sud de III croûte océanique : 6) la slratigraphie sismique montre que 'e~ sédiments du Golfe duns les zoncs de croûte transitionnelle rcprésentent une évolution verti C.tle depuis Ics volcanÎtes el les sédiments continentllux, y compris le .c; évaporites. vers des faciès marins de faible profondcur. pui ~ de ~ ~éd imcn u à grande profondeur de dépôt. ces dcrniers reposant directement sur la croûte océanique dans le Golfe central. Ces données suggèrcnt le schéma d ·évolution suivllnt : le balo~ in initial currespondant au Golfe du Mexique a évolué comme une marge continenHlle di vergente (passivc). il la même époque et ~ ui vant Ics mêmes m écanis me ~ que la marge nord-atlantique. y compris la formation de croûte océanique. Nous suppoMlns qu·une "hase d~ distension ("·rif"·) Trillssico-Jurassiquc a élé accomp:lgnée d·un bombement générali sé. une distcnsion el un comblemcnt de bassins de rift par dc ~ volcaniles CI des roches d·origine terre ~ lre lor~ que I"Amérique du No rd s·esl séparée de I"enscmblc Afrique-Amérique d u Sud. La formaI ion de la croûtc de transition amincie a eu lieu ~ndanc celle période. Pendant rultime ét,lpc de celle phase (Jurassiq ue moyen-supérieur) le Golfe ~ ·cst morcelé cn une sérÎe de bassins subsidencs séparés: dans ce rlain ~ d·entre eux. un épaiS horizon de sel s·e,t déposé dans un environnement marin de faible profondeur. Une phase dt s'Ibsidence el de dlpfacemeJ/l C·drif"" IL débuté au Jurassique supérieur. iJ y a environ 150 millions d·annécs avec une di~ten s i on majeure du Golfe ce ntral et la formation d'une croûle océanique nou velle. Le bloc Vucatnn 5·eu probablement déplH cé " c("Illi, rAmérique du Nord suivant une dircction NO-S É parallèle aux failles trllnsformantes de l' Atlantiquc Nord. en séparant le ba s~in salifère de chaque côté de la nouvelle croûtC océaniquc. L·accrétion fut aplXlremmenl brèvc. mais le bassin a continué à subsider rapidcment du fait du refr o id i~~emcnl de la lit hosphère. La s ub~idenee IL été accompagnée d ·un fluage par gr:t\'ilé du sel daM le bassin et de la mise en place d·une marge carbonatée toul le long d·une Lo nc tectonique charnière à la périphérie du bassin. Des sédiments d ·eau peu profonde il profonde sc sonl dépo~és le long des margcs du bassin . landis que seuls des sédiments de grande profondeur se sont déposés dans le bassin océanique nouvcllcmcnl créé. L ·évolu tion initiale du ba~s in s·cst tcrminée au Créweé moyen. °lur, d·un ,hénement dïmport;;nce majeure ~ouligné par unc forte discontinuité à I"échelle du Golfe lout entier. L3 sub~idence 101:'llc du bassin depuis la formai ion de la croÎlle océanique a été supérieure à 10 km. cn partie à cause de la charge ~é dimenl;tire et en pilrlic à cause du refroidissement de ln lithosphère. Ocea nol. A ("((j, t981 . Acles 26'COnllrès Jnternation'II de Géologie. colloque GéOlogie des marge ~ conlÎnentalcs. Paris. 7-17 juil. 19S0. 120,1·136. INTRODUCT ION Reccnt plaie re eons tru ç .ion ~ ba~ed o n paleomagnctic data suggest various Triassic-Early Jurassic ovcrlap~ o f South The Universil y of Tc xa~ Marine Scicnce Instilute­ America with ccntral Mexico. Vuca",". and portion~ o f Ihe GalveMon Geo("lhysics Laboratory - (UTMSI-GGL) began Gul f (Ladd , 1976 ; Va n der Voo el al. 1976 : Pilger. 1978 : in 1974 a Jong-Ierm project 10 study the geologic hi ~ t ory of Gosc et ai .
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