Tracking diagentic history in mixed volcanic and

reefal sedimentary system in Triassic-Jurassic

transition sequence in the northern Israel subsurface

Dorit Korngreen, Yehudit Harlavan

Report GSI/08/2016 Jerusalem, January 2016

Ministry of National infrastructures

Energy and Water Resources

Geological Survey of Israel

3

Contents ABSTRACT ......................................................................................................... 5

1.INTRODUCTION .............................................................................................. 6

1.1 The association of volcanic and carbonate rocks ............................................ 6

1.2 Sr stratigraphy .............................................................................................. 9

1.3 THE AIMS OF THIS WORK ...................................................................... 11

2.GEOLOGICAL SETTING ................................................................................. 11

3.METHODS ....................................................................................................... 13

3.1 Sampling and sample preparation ................................................................. 13

3.2 Cathodoluminescence (CL). ......................................................................... 13

3.3 Sr stratigraphy ............................................................................................. 14

4 RESULTS ......................................................................................................... 15

4.1 ASHER-ATLIT BOREHOLE (5600 – 5450m) ............................................. 15

4.1a Biostratigraphy ...................................................................................... 15

4.1b Reefal and Algal facies in the intermittent carbonate horizons .................. 15

4.1c 87

Sr/86

Sr ratio and chronostratigraphy ...................................................... 19

4.2 ELIJHA-3 BOREHOLE (2700-2950 m) ....................................................... 23

4.2a Biostratigraphy ...................................................................................... 23

4.2b Algal-mats and ooids facies in the post volcanic platform in Elijha 3

borehole. ...................................................................................................... 24

4.2c The 87

Sr/86

Sr ratio .................................................................................. 26

4.3 GA’ASH 2 BOREHOLE ............................................................................. 28

4.3a Cathodoluminescence (CL) .................................................................... 28

4.3b Biostratigraphy ...................................................................................... 28

4.3c The 87

Sr/86

Sr ratio .................................................................................. 31

5. DISCUSSION .................................................................................................. 34

5.1 Assiniging numerical age to the boreholes .................................................... 34

5.2 The T-J transition Biostratigraphy ................................................................ 36

5.3 Facies recorded in the late Triassic to early Jurassic, northern coastal plain of

Israel ................................................................................................................ 37

5.4 Pangea rifting and the reefal facies. .............................................................. 39

6.CONCLUSIONS ............................................................................................... 40

REFERENCES .................................................................................................... 43

APPENDIX ......................................................................................................... 48

4

List of Figures:

Figure 1 Paleogeographic reconstruction of the Late Triassic ................................... 7

Figure 2: Map location of the boreholes penetrated the Triassic strata in Israel. ......... 8

Figure 3 : The 87

Sr/86

Sr ratio of the oceans at the deep-time past ............................ 10

Figure 4: Foraminifers mentioned in text ............................................................... 17

Figure 5: Interval 5600-2350 m depth in Asher Atlit 1 borehole. ............................. 18

Figure 6: Late Triassic reef Facies Asher Atlit 1, interval 5265 – 5180 m depth.. ..... 19

Figure 7: Asher Atlit 1 Borehole 87

Sr/86

Sr ratio values in 5600 - 5445 m interval. .... 20

Figure 8: Correlations of major elements. .............................................................. 21

Figure 9: The values of 87

Sr/86

Sr ratio in 5600 - 5450 m interval of Asher Atlit 1

borehole ............................................................................................................... 22

Figure 10: Foraminifera recovered from interval 2199-3002 m in Elijah 3 borehole. 24

Figure 11: Log Elijah 3: lithology, Sedimentary components, foraminifera .............. 25

Figure 12: Elijh Borehole, Sr87

/Sr86 ratio versus depth. .......................................... 26

Figure 13: The 87

Sr/86

Sr ratio of 2700-2950 m depth interval in Elijah 3 borehole. ... 27

Figure 14: CL of 4422 – 4451 m samples in T-J transition interval at Ga’ash 2. ...... 29

Figure 15: Composite log of interval 5030- 4300 m depths in Ga’ash 2 borehole ..... 30

Figure 16: Ga’ash Borehole, Sr87

/Sr86

ratio versus depth. ....................................... 31

Figure 17: The 87

Sr/86

Sr ratio of 4400-4600 m depth interval in Ga’ash 2 borehole .. 32

Figure 18: Facies of the Triassic – Jurassic transition in Elijah 3 and Ga’ash 2

boreholes ...................................................................................................................... 33

5

ABSTRACT

The major aim of this research is to characterize the Triassic-Jurassic transition in the

subsurface of western northern Israel in terms of biostratigraphy, depositional

environments, diagenetic processes, and when possible to assigned numeric ages

using Sr stratigraphy method. Three boreholes were chosen two that include volcanic

activity (Elijah 3 and Asher Atlit 1), and one without (Ga’ash 2). This work made the

first regional attempt to define the T-J transition in the subsurface of northern Israel

by 87

Sr/86

Sr ratio chronostratigraphy, anchored by the biostratigraphy when it was

available. Some 240 thin-section of boreholes’ cuttings in total were examined for

micropaleontology and paleo- depositional environments analyses by PL and CL

microscopes. In addition, from the same intervals, 140 samples were analyzed for

87Sr/

86Sr ratio along with elemental analysis. It can be concluded that applying Sr

stratigraphy can be done on boreholes but extra care should be taken when calculating

the age. In Elijah 3 borehole, the T-J transition is positioned at 2855 m depth, above

the volcanics, and above the base of Nirim Fm., indicating Late Triassic pulse of

volcanism with no later volcanic activity. In Ga’ash 2 borehole, the results yield early

Jurassic ages (197 Ma) at depth of 4532 m, but the T-J transition couldn’t be

identified. Finally, In Asher Atlit 1 borehole, an upper interval of reefal environment

was identified using Pl and Cl microscopes, indicating strong connection between

occurrence of reef environment and the volcanic activity. Based on the biostratigraphy

it can be concluded that the T-J boundary is this borehole is up higher than previously

thought. The Sr stratigraphy failed to predict ages probably either because of the poor

constrains of the samples themselves or more probably as a result of the associated

volcanism. The Late Triassic transitioned into the Jurassic found in Elijah 3 and

Ga’ash 2 boreholes, display similar and typical deposition environments of relatively

proximal carbonate environment which is composed of algal mats and ooids

preceding, during and post the transition. These observations are similar to the

extensive stromatolitic limestones of the inner shelfs of the Late Triassic of the Alps

and the entire Tethyian shallow environments. This wide-scale carbonate platform

during the T-J transition (where no sedimentary gaps were recognized yet) may

specifically affirm that regionally, the T-J transition had occurred during volcanic and

tectonic quiescence, probably at the turning point from active rifting to basin sagging.

6

1. INTRODUCTION

1.1 THE ASSOCIATION OF VOLCANIC AND CARBONATE ROCKS

The T-J transition is one of the five major Earth-Life Transitions (ELT) of the

Phanerozoic Earth history that characterized by decreasing in speciation in the seas

where 34% of the marine genera vanished and ammonoids, brachiopods, bivalves,

gastropods, reef building corals, sponges and foraminifera were sever reduced (e.g.

Flügel, 2002; Stanley, 2003). On land, all pseudosuchians and many of the large

amphibians became extinct. The cause of this mass-extinction, remains under debates,

but the general scheme is that the T-J transition had happened during the major

breakup of Pangea, associated with volumetric volcanic eruptions, and followed by

the failure of the carbonate factory.

Large igneous activity consisted mainly of eruptions of basalts in flows and dykes

preceded the breakup of Pangaea near the end of the Triassic and at the early Jurassic

period. This activity is linked to the initial formation stages of the Atlantic Ocean

generally termed the “Central Atlantic Magmatic Province” (CAMP; Fig. 1). The

CAMP expanded over northeast South and southeast North America, northwest

Africa, and southwest Europe. It is widely excepted that it had begun 201 million

years ago and lasted for over 0.6Ma (Blackburn et al. 2013), and is tied to the

Triassic–Jurassic (T-J) extinction event (e.g. Pálfy, 2003; Olsen et al., 2003; Marzoli

et al., 2004; Galli et al., 2005; Schoene et al., 2010; Whiteside et al., 2010). Whiteside

et al. (2007) estimated based on following δ13

Corg, that the palynological extinction

might precede the oldest CAMP flow. Since contemporary rifting of the Late Triassic

and Early Jurassic is known to underlie many southern Tethyan and as well on the

Levant margin, the Late Triassic – earliest Jurassic (T-J) volcanism is frequently tied

to tensional basins.

Because of that, the T-J transition events and the associated volcanism is at the heart

of many recent researches tying the Triassic and the Early Jurassic mass extinction to

a climate crisis associated with the activity of the CAMP.

7

Figure 1 Paleogeographic reconstruction of the Late Triassic (reconstructed by Ron Blakey, NAU

Geology), shown are the known range of the CAMP, Proto-Atlantic and Tethyan rifting and the area of

this research.

Late Triassic and early Jurassic successions in Israel are mostly known from the deep

subsurface (Fig. 2) but are exposed in few outcrops in the Negev and in the Hermon

region (Mouty, 2000). While in northern Israel the base of the Jurassic succession was

considered as associated with volcanism, in other areas, the T-J boundary is truncated

and covered by lateritic palaeosols and is considered to be post-erosional exposure

features with no volcanic contribution (Mish'hor Fm; Goldberg, 1964; Goldbery,

1979). In in the Negev, the post Triassic lithostratigraphy begins with the pedogenic

lateritic Mish’hor Fm (Heller-Kallai et al., 1973, Goldbery, 1982) overlaid by Ardon

Formation with considerably wide stratigraphic gap of 28 Ma (Buchbinder and le

Roux, 1993); in the southern coastal plain, the Brur Formation is overlaid the

Mish’hor Formation (Nevo 1963; Goldberg, 1964; Derin, 1974). Northward, the

lateral carbonate suites associated with dolomite and evaporites overlaid the Triassic

section of Qeren and Haifa Fms (Hirsch et al., 1998) which are timed to accumulate in

rifting period. The thick carbonate platform, up to 1500 m that overlaid the Asher

volcanics (see 1.1.2.) in northern Israel and in the central coastal plain defined as

Nirim Formation (Derin, 1974, Hirsch and Picard, 1988), and following this definition

was identified in Elijah 1-3 and Ma’anit 1-3 boreholes also. This formation is

considered as the northward- westward equivalent of the southern dominant to

bearing siliciclastic formations (Mish’hor, Ardon, Inmar and Daya), and were

assigned to the Pleinsbachian (lower Nirim - Derin, 1974) and Torcian - Aalenian

(Upper Nirim, Derin and Reiss, 1966; Derin, 1974).

8

Figure 2: Map location of the boreholes penetrated the Triassic strata in Israel. The three studied

boreholes in this work (northern Israel) are marked by a square: among them, only Ga’ash 2 borehole is

absent volcanism in the T-J transition. Volcanism had been tracked in Meged 2 and Ma’anit 1-3 prior

to T-J transition and in Devora 2, the volcanics assigned to Late Jurassic-Cretaceous volcanic phase.

About 2500 m thick mostly basaltic succession is penetrated by the Asher Atlit 1

borehole and the volcanics were named “the Asher Volcanics” (Dvorkin and Kohn,

1989) and was related to a Mesozoic phase of rifting and development of a deep basin

with a possible ocean-like crust between the Levant and the Tauride block (Ben-

Avraham and Hall, 1977; Garfunkel and Derin, 1984; Garfunkel, 1989). The oldest

age found in Asher Volcanics is 202 ± 4 Ma, and 206.8 ± 3.0 Ma for one sample

(cuttings, ~4840 m; Kohn et al., 1993), but comprehensively, the volcanic section as a

whole was assigned to an Early Jurassic phase (Gvirtzman and Steinitz, 1983).

9

Thinner sections of Asher volcanics were penetrated also in other boreholes (Haifa 1,

Rosh-Pina 1 and Yagur 1 boreholes) and all were assigned to the early Jurassic age,

and are all overlaid by the Nirim Formation (assigned to Pleinsbachian of the early

Jurassic).

The base of the Volcanic Asher succession interlayered with thick carbonates interval

and was assigned to the Late Triassic (Carnian-early Norian; Korngreen and

Benjamini, 2001, 2011). The carbonates shows a development of reef and circum-

reef facies, that had interbedded with volcanics eruptions and which indicating reef-

volcanic genetic connection (Korngreen and Benjamini, 2001) very similar to other

paleo-seamount and rifting phases associated with reefs around the Tethys in the Late

Triassic, such as the parts of the Dolomites (Bosellini and Rossi, 1974), Oman (Searle

and Graham, 1982), Antalya (Robertson, 1993) and Tibet (Fu et al., 2010). The upper

part of the volcanic section (3000-4800 m depth interval) which was attributed to an

early Jurassic volcanic phase (Gvirtzman and Steinitz, 1983, Khon et al., 1993) is

absent of intermittent carbonate horizons and had been described as exchanges of

basalts and clayey horizons (Sherman, 1983). In addition, the volcanic sequences that

had been previously attributed to Asher Volcanics in Devora 2, Haifa 1, Rosh-Pina 1

and Yagur 1 boreholes, actually were assigned to a much younger and different later

magmatic phase. Recently, 1000 m above the base of the reefal/volcanic sequence of

Asher Atlit 1 (at about 4840 m depth) yield a zircon-based Late Triassic (late Norian)

age of 205.5 - 206.5 Ma (Golan, per. comm., Katzir et al., 2015).

1.2 SR STRATIGRAPHY

Strontium is homogeneously distributed in the oceans due to its long residence time of

4*106yr (Holland, 1978), but the isotopic composition of Sr (

87Sr/

86Sr ratio) in the

oceans is known to fluctuate since the beginning of the Phanerozoic eon.

Measurements of the87Sr/86

Sr ratio in the ocean by numerous studies were integrated

to plot the change of this ratio with time. This plot is based on measurements of

the87

Sr/86

Sr ratio in biogenic carbonates, and the Sr isotopic composition is used for

chronostratigraphic correlation of marine sediments, based upon the 87

Sr/86

Sr

variation of the ocean’s water with time. Smalley et al., (1994) introduced a statistical

method for fitting a curve to the available data using Weighted Scattered plot

Smoother (LOWESS) software. The software uses ca. 4100 data pairs (age - 87

Sr/86

Sr

ratio), data screening, corrections for inter-laboratory bias and overlap segmentation.

10

The assigned age is within 95% confidence meaning 0.000001 intervals for the

87Sr/

86Sr ratio. Most important are the prospective candidates for determining the Sr

isotopic composition of the ocean water at the time of deposition; belemnites,

brachiopods shells, carbonate cement, foraminifera (calcite) and conodonts, provided

that they show no evidence for alteration or diagenetic processes. Nevertheless, in this

study, in the absence of such candidates we use the carbonate rocks with attention to

the fact that they may had gone some diagenesis. The stratigraphic age is calculated

using comparison to the updated compilation by McArthur et al., 2012 (LOWESS:5;

Fig. 3).

The age of the Triassic-Jurassic boundary is widely accepted at around 200 Ma (e.g.

Gradstein et al., 2004). Based on samples from localities around the globe, the

compiled curve predicts the actual seawater 87

Sr-86

Sr ratio as a function of time for

this period. Increase in the rate of decline of the seawater curve from mid-Norian

probably corresponds with the development of the Atlantic spreading center in the

Mid - Jurassic. The 87

Sr/86

Sr ratio of the ocean 200 Ma ago was ca. 0.7075 while that

of the T- J boundary is ca. 0.7076 (Koepnick et al., 1990, McArthur et al., 2012). This

ratio reflects the tectonic, eustatic and climatic changes during this period. One

important change was the breakup of Pangea which led to seafloor spreading

accompanied by hydrothermal circulation of seawater through oceanic crust.

Following the approach, carbonate deposited during the T- J boundary period should

yield 87

Sr/86

Sr ratio of ca. 0.7076 (Fig. 3).

Figure 3 : The 87

Sr/86

Sr ratio of the oceans at the deep-time past following Koepnick et al. (1990),

McArthur et al. (2012).

11

1.3 THE AIMS OF THIS WORK

The major goal of the current study is to characterize the Triassic-Jurassic transition

in the subsurface of northern Israel, by analyzing cutting material recovered from

three boreholes: Asher Atlit 1, Elijah 3 and Ga’ash 2. In specific:

1. Characterize the biostratigraphy and depositional environments in the T-J

transition.

2. Identify diagenetic processes in carbonates that can be associated with

volcanic fluids.

3. Describe the affinity of the physical processes with the regional T-J transition.

4. Making first regional attempt to define the T-J transition in the subsurface of

northern Israel by 87

Sr/86

Sr ratio chronostratigraphy.

5. Illuminate to some extent, the affinity between the regional sedimentary record

and its extirpations with the regional volcanism.

2. GEOLOGICAL SETTING

The chosen boreholes in this study, is each is important as described below:

The Atilt- 1 borehole is located at coordinates EI4425I/N234500 (Israel Grid), and

was drilled in stages between 1981 and 1983. Unpublished reports on this borehole

are by Cousminer (1982), Gerry and Derin (1981) and Sherman (1983). The section

under focus was placed biostratigraphically at the Late Triassic, based on ostracods

(Gerry and Derin, 1981), by palynomorphs (Cousminer, 1981), and by foraminifers

(Korngreen and Benjamini, 2001). The section that composes of basaltic volcanics

and reefal carbonates is unknown from the other Triassic outcrops of the Negev, Sinai

and Jordan but the association of carbonates interbedded with volcanics was found in

many thick Triassic successions around the Tethys. The T- J transition in Asher Atlit

1 borehole is in the absence of any equivalent to Mis’hor formation was determined at

the transition into the massive part of the volcanic succession at 5464 m depth.

The Ga’ash 2 borehole was drilled in 1980-81 in the coastal plain of Israel (coord:

N181435, E133836) by Oil Exploration company, on what is today an elevated block

bounded by two faults directed NW–SE (Garfunkel, 1998; Gardosh and Druckman,

2006). The borehole penetrated Late to Middle Triassic carbonates and shales in the

interval from 4583–5505 m. The Triassic strata in Ga’ash-2 have a significantly

reduced thickness in comparison with other Triassic succession in Israel (Druckman,

12

1974). Bio- and chronostratigraphy was reported by Korngreen and Benjamini (2006).

This borehole is marked at 4560 – 4595 m depth by about 35 m of colored shale and

clay (core 1) interpreted as “…deeply weathered residual detritus including

mineralized vascular tissue strands…” (Cousminer, 1981) and was assigned to

exposure event and to the Mish’hor formation equivalent. Following that, the overlaid

carbonates were assigned to the Jurassic Nirim Fm. (Gvirtzman et al., 1984), although

no other identical microfossils were recovered at the base of the formation.

The Elijah 3 borehole site is located on the northern coastal plain of Israel near Mount

Carmel, between Caesarea and Haifa, in the banana orchards of Kibbutz Ein Karmel,

eastward to Road 40. The borehole was drilled by Zion Oil & Gas Company, 2009,

2012 and sealed at 2013. Three rock types were found to dominate the volcanic

section (530 m) of the Elijah 3 borehole (following Golan, per. comm.; Katzir et al.,

2015): dolerite (at 2909 2906 m interval), olivine basalt and seriate basalt to the

borehole base (3332 m depth). A transition zone of mixed layer volcanic-carbonate

interval overlaid the volcanic succession (2906-2873 m depth), and a sequence of

carbonates above it. Previously, the carbonate samples from the 2199-2702 m

interval of Elijah 3 borehole (~800 m) had been studied briefly by thin sections made

at 100 m intervals of the borehole cuttings (Korngreen et al., 2010). The borehole

penetrated a primarily carbonate section underlain by volcanics (considered as Asher

Volcanics; 2897-3002 m interval). The deduced age for the carbonate section was

Aalenian - Bajocian according to foraminifera and palynomorphs, and the absence of

dinocysts. Intra Jurassic subaerial exposure event was identified at depth 2500 m, and

the downhole transition from carbonates to volcanics was characterized by a

monomictic micro-breccia, possibly marking contact with volcanic fluids, and loosely

packed dolomite interleaves. The carbonate facies immediate above the volcanic

section indicate a marine carbonate platform developed with indications to shifting

from outer ramp through high-energy shoals, to restricted peritidal nearshore

environments and was assigned to Nirim Formation.

Recent dating the top of the volcanics at the borehole base to the latest Triassic (ca.

200 Ma; Katzir, Golan et al., 2015), encourage to look for the T-J transition above the

magmtic section.

13

3. METHODS

3.1 SAMPLING AND SAMPLE PREPARATION

In general, the sampled material of this work was produced as the rock was

fragmented while a drill bit had been proceeding through the interval. The rock

fragments (“cuttings”) were pumped up-hole by the drilling’s circulating cooling

fluids and mud; following their monitored rate of circulation and their viscosity, the

sample’s depth was deduced by calculation, each sample typically, are caught or

collected as composite samples that reflect the various lithologies drilled over 3 m

interval. To keep on with good monitoring of the subsurface, the borehole should not

lose water, and any stop of the pumping or the drilling can cause fluids and material

lost or mixed with other intervals. Moreover, weakly consolidated rocks will change

the rate of circulation, subsurface caves might cause loss of circulation and material

will not reach the surface; highly brittle rocks (e.g. volcanics) might be erode easily

and may fall downhole (caved) or to be re-transported up hole by the mud circulation

and may attribute to different depths. Many is relying on the well-sitter skills, as the

fragments themselves should be treated in highly cautions when they drop out of the

borehole into the settling pits and when they isolated from the mud; although these

descriptions and the derived uncertainties that fragments might be out of their original

locations, it should be always considered, that in absence of recovered cores, the

majority of the material fragments are the only direct physical lithological data for

examination and analyzes deep subsurface intervals, and general trend in any of the

results will help to avoid mistakes, and to display the sample at its approximate

relevance.

Ca. 240 thin-section of boreholes’ cuttings in total were examined for

micropaleontology and paleo- depositional environments analyses; for Elijah-3, 40

were new made and 11 from the archive; for Ga’ash 2, 75 were new made and 21

from the archive; for Asher Atlit 1, 71 new made and 20 from the archive. Thin

sections were examined by petrographic microscope and documented by a digital

camera for foraminifers, skeletal and non-skeletal components identification.

3.2 CATHODOLUMINESCENCE (CL).

The slides were examined under CL microscope CITL-mk5 mounted on Olympus

petrographic microscope to observe features visible through their diagenetic overprint.

14

Use of CL is justified by luminescence features imparted during crystal growth by

incorporation of trace amounts of elements; Mn++, Fe++, are most common in

sedimentary system; the Mn+2 is the most important activator ion of CL, while the

ion Fe+2 is a luminescence’s quencher (e.g. Pagel et al., 2000), when Intensity of

luminescence can depend on the Fe/Mn ratio, and their incorporation into the lattice is

dependent on the Eh conditions (Pierson, 1981; Richter and Zinkernagel, 1981; Frank

et al., 1982, etc). Exotic luminescence occurs when rare activated ions, or common

ion in are present in the participating solution effected by hydrothermal or volcanic

3.3 SR STRATIGRAPHY

Some 140 87

Sr/86

Sr ratio analyses were carried out on the boreholes’ material based

on one grain of the chips (the fragments of the rocks) from each sample interval at

selected studied interval: 33 of Asher Atlit 1 at the base of the volcanic succession; 44

samples from the T-J transition at Ga’ash 2 and 62 samples of the T-J transition at

Elijah 3. Chips were chosen under binocular and handpicked carefully to consist of

calcite as much as possible. Chips were rinsed using distilled water to remove any

borehole mud and then placed in a 50 ml clean tube (ca. 0.1gr). Selective dissolution

of carbonate (calcite or dolomite) was accomplished by using ultra clean 0.5M acetic

acid. Dissolution took place under room temperature for 24 hours until no release of

CO2 could be observed. The solution was then separated from the residual and dried

using clean Teflon beakers on hot plate under clean condition. The salt was dissolved

by 0.1 HNO3 ultrapure-acid and prepared for elemental analysis. An liquate was used

for elemental analysis of Al, Si, Ca, Mg, K, SO4, Sr using ICP-AES at the Geological

Survey of Israel. The Sr isotopic ratio analysis followed

The isotopic composition of Sr was measured using a Nu Plasma MC-ICP-MS

instrument. Mass discriminations were corrected using repeated measurements of the

SRM-987 standard. The long-term precision of isotopic ratio determination (2

relative standard error) was 0.002% for 87

Sr/86

Sr.

15

4 RESULTS

The Elemental chemistry, 87

Sr/86

Sr ratio and assigned ages when relevant appear in

the appendix.

4.1 ASHER-ATLIT BOREHOLE (5600 – 5450M)

4.1a Biostratigraphy

The base of the studied section in this borehole (5464–5481 m) recovered

foraminiferal species indicating Carnian – Rhaetian age (Korngreen and Benjamini,

2001): Aulotortus pokornyi - Norian– Rhaetian (Piller, 1978); Amphorella

lageniformis – Carnian – Norian (Salaj et al., 1983). These two species were

associated with Diplotremina sp.; Endothyra sp.; Valvulina sp.; Meandrospiranella

irregularis. Following the foraminifera assemblage, the Carnian – Norian transition

occurred at about 6260 m depth (Korngreen and Benjamini, 2006). The thick

sequence of volcanics overlaid this interval were assigned to the Early Jurassic

(following broad agreement of Jurassic age of the volcanics; Gerry and Derin, 1981;

Cousminer, 1982; Lang and Steinitz, 1989; Kohn et al., 1993; Korngreen and

Benjamini, 2001).

Following the novel radioactive dates from the main phase of Asher Volcanics

(Golan, per. comm., Katzir et al., 2015), work was focused on the intermittent

carbonate intervals in the massive continues volcanic section (Figs. 4 and 5). The

recorded foraminifera of this work were Aulotortus tumidus (late Norian – Rhaetian

(Mancinelli et al., 2005); Fig. 4, 5-6), associated with Dustominidae (Late Triassic; Pl.

1, 2) Earlandia sp. (Fig. 4, 3-4), Agathammina sp. (Fig. 4, 10), Planiinvoluta sp. (Fig.

4, 9), Ophthalmidium sp. (Fig. 4, 7) and Endothyra sp. (Fig. 4, 8) in 5260-5180 m

depth interval; in 5212-15 m depth interval, a Late Triassic (Norian) Urnulinella cf.

andrusovi (Fig. 4, 1) was recorded, considered as a typical reefal foraminifer

(Chablais et al., 2011;). The first “Siphovalvulina” sp. that usually marks the Triassic

– Jurassic transition occurred at depth 2780, bur more work need to be done on this

interval. The foraminifers’ assemblage of these intervals is matching the evaluated

Norian age of the Interval.

4.1b Reefal and Algal facies in the intermittent carbonate horizons

Fig. 5 shows the log of the interval 5600-2350 m depth in Asher Atlit 1 borehole

comprises the T – J transition. The log displays radioactive dates (Golan, per.

comm.), lithology, micro-sedimentary components and recovered foraminifera from

16

previous and this works. Since some of the work is still under processing and

studding, not all the planed results are included in this report, but they will be

integrated in a final one.

The base of the volcanic sequence is inserted in carbonate and volcanics exchange

interval (5400-5600 m depth) briefly described in Gerry, 1983 and in details in

Korngreen and Benjamini (2001) as Late Triassic reefal and volcanic association.

Examination of the carbonate dominant interval overlay 125 m thick of separating

entirely volcanic sequence (85 m thick; 5265 – 5180 m depth) found to be composes

also of Late Triassic reef components and foraminifera, extending the intimate

interlayering alternations of extrusive volcanism and reef establishment from the base

of the volcanic succession at about 6250 m depth up to 5180 m depth – 1070 m,

before the volcanism become the dominant lithology upwards (up to 3000 m depth,

2180 m of volcanic activity). The interval contains also recrystallized reef biota of

coral origin, sponge structures, typical reef acicular structure, Microtubus, alveolar

green algae structure, foraminifera, algal binding, and vesicular structure all trapped

by micrite (Fig. 6, 1-8). Under the CL, exotic bright luminescence indicating

carbonate cement fills under volcanic fluids effect (Fig. 6, 1-2). Reef debris found to

be associated with volcanic lithoclasts (Fig. 6,7) indicates adjacent volcanic sea

mount stabbed out of the sea level.

17

Figure 4: Foraminifers mentioned in text: 1. Urnulinella cf. andrusovi ; (Samuel and Borza, 1981);

Carnian; Asher-Atlit 1 5212 -15. 2. Dustominidae; Asher-Atlit 1 5212 -15. 3. Eaerlandia sp.; Asher-

Atlit 1 5229 -32. 4. Eaerlandia sp.; Asher-Atlit 1 5233 -36. 5. Aulotortus tumidus; Asher-Atlit 1 5233 -

36. 6. Aulotortus tumidus; Asher-Atlit 1 5240 -43. 7. Ophthalmidium sp.; Asher-Atlit 1 5240 -43. 8.

Endothyra sp.; Asher-Atlit 1 5233 -36. 9. Planiinvoluta sp.; Asher-Atlit 1 5240 -43. 10. Agathammina

sp.; Asher-Atlit 1 5243-46. 11. Unidentified foraminifer; Gaash-2 4400-03. 12. Turrispirilina sp.?;

Gaash-2 4400-03. 13. Endothyranella sp.; Gaash-2 4400-03. 14. Aulotortus sp.; Gaash-2 4416-28. 15.

Tetrataxis sp.; Gaash-2 4425-28. 16. Valvulinids; Gaash-2 4428- 40. 17. Siphovalvulina sp.; Gaash-2

4428- 40. 18. Tetrataxis sp.; Gaash-2 4458- 40. 19. Oberhouserella sp. Gaash-2 4458- 40. 20.

Austrocolombia sp.; Gaash-2 4660- 03. 21. Pilamminella kuthani; Gaash-2 4657- 60. 22. Pilamminella

kuthani; Gaash-2 4621- 24. 23. Siphovalvulina sp.; Asher-Atlit 1 2439 -42. 24. Valvulina metula or

Textulariopsis sp.; Gaash-2 4325- 28. 25. Miliolids; Gaash-2 4325- 28. 26. Paleomayncina termieri

(Hottinger) or Endothyra sp.; Gaash-2 4325- 28. 27. Orbitopsella praecursor? (Gümbel); Gaash-2

4470 (caved). 28. Lituosepta compressa Hottinger; Gaash-2 4340- 43.

18

Figure 5: Interval 5600-2350 m depth in Asher Atlit 1 borehole comprises the Triassic – Jurassic

transition. 1 – Age used in this work is following preliminary results of radioactive dates after Golan,

per. comm., Katzir et al., 2015; Age in previous works is after Derin and Gerry, 1981; Sherman, 1983.

The T-J transition in this interval is preliminary determined following the results in Ga’ash 2 and Elijah

3 boreholes. Lithology column shows dominant volcanics and some smaller intermediate carbonate

intervals. Micro-sedimentary components and recovered foraminifera displayed by the lithology. Note

that 1250 m of entire volcanisc exchange with clayey horizons sequence had been cut off from the log.

19

Figure 6: Late Triassic reef Facies Asher Atlit 1, interval 5265 – 5180 m depth.1. Sparry mosaic in

recrystallized reef biota, with trapped micrite; sample 5257 – 60. 2. Same sample under CL, exhibiting

very exotic bright luminescence (BCL) cement fill of zooid (Z) and other caves (C), indicate volcanic

fluids effect; sample 5257 – 60. 3. Biolithite of coral origin, vesicular structure, micrite and bioclasts

debris fill cavities; sample 5255 – 57. 4. Calcified sponge structure; sample 5237 – 40. 5. Acicular

structure (Ac) in biolithite; sample 5233 – 36. 6. Recrystallized structures of biolithite of coral origin

with microtubus (M) and other encrusting organisms fill cavities with peloidal micrite; Sample 5233 –

36. 7. Recrystallized structures of biolithite of coral origin with peloidal micrite fill. Among the clasts

are volcanic lithoclasts (V) mentioned also in Garfunkel (1983); sample 5233 – 36. 8. Alveolar (Al)

structure probably of green algal origin with sponge structure (S), porcelanous foraminifer (F) and

other bioclasts debris reef-derived, with foraminifera and algal binding; sample 5253 – 56.

4.1c 87

Sr/86

Sr ratio and chronostratigraphy

In the first stage, two set of sub-samples of carbonate appearances were isolated from

a depth of 5566 m. The first subset consists of grey chips while the second consist of

white chips. This was done in order to determine the preferred type of sample to

handpick and analyze. These rock chips were dissolved using acetic acid and the

87Sr/

86Sr ratio was measures. The preliminary results indicated a wide range of values

from the same depth and in general a higher 87

Sr/86

Sr ratio for the white chips (Table

20

3, Appendix). Since the elemental chemistry was not determined at that stage the

white chips were chosen for further work.

In the second stage a set of ca. 45 samples were analyzed for Sr isotopic composition

and elemental chemistry (Table 4, Appendix). In this case, the elemental chemistry

was determined and the percent of anhydrite, dolomite and calcite in the solutions

were calculated. Calculations were done in the following order, first the % dolomite

using the Mg concentrations, and then the % anhydrite using the SO4 concentrations

and finally the %CaCO3 after subtraction the Ca associated with dolomite and

anhydrite (Table 4, Appendix). No correlation was found between one of the major

constitutes of the dissolve sample (i.e. Ca, Mg, 1/Sr and SO4) and the 87

Sr/86

Sr ratio,

which suggests no mixing of phases.

Not like Elijah 3 and Ga’ash 2 boreholes, no systematic was observed for this section

(Fig. 7). A more detailed study shows that Sr concentration has good and positive

correlation with Ca and SO4, which may suggests contribution from anhydrite that is

known to consist of thousands of ppm of Sr (Fig. 8). However, the minor amount of

anhydrite (less than 1%) is probably not enough to alter the 87

Sr/86

Sr ratio. Fig. 9

shows the inconsistent pattern of the values distribution with the world curve,

excluding 8 samples that shows fitting with the Norian – Rhaetian curve, in agreement

with the micropaleontology indications.

Figure 7: Asher Atlit 1 Borehole 87

Sr/86

Sr ratio values in 5600 - 5445 m interval. No systematic can be

observed.

0.7068

0.7070

0.7072

0.7074

0.7076

0.7078

0.7080

0.7082

0.7084

0.7086

5400 5450 5500 5550 5600 5650

87

Sr/8

6Sr

Depth m

21

Figure 8: A good correlations between Sr, Ca, Mg and SO4 concentrations in the dissolutions

suggesting that carbonate dissolution was accompanied by anhydrite dissolution

Figure 9: The values of

87Sr/

86Sr ratio in 5600 - 5450 m interval of Asher Atlit 1 borehole (yellow) on the global curve of McArthur et al., 2012. The values distribution

shows no consistency with the world Curve excluding a quarter of the values (8 samples) that fit the Norian – Rhaetian curve.

4.2 ELIJHA-3 BOREHOLE (2700-2950 M)

4.2a Biostratigraphy

Previous work on the 2199-3002 m interval of the borehole (~800 m. thick;

Korngreen et al., 2010) yield age Aalenian - middle Bajocian (Jurassic) to 2199-2702

m depth mainly by palynomorphs. This interval was associated with valvulinids and

glomospirids, and the actually first appearance of Lucasella sp., Orbitopsella

praecursor, and the planktonic foraminifer "Protoglobigerinid" was at 2700 m depth.

The depositional environments of the 2199-2702 m interval shifted from below

FWWB on the ramp (valvulinid mudstones), through high energy shoal barriers,

restricted peritidal proximal environments, to nearshore supratidal environments. A

Subaerial exposure event was identified at 2498-2502 m in fenestral bindstones of the

peritidal sequence. Monomictic microbreccia indicating contact with volcanic fluids,

and loosely packed dolomite crystals suggest replacement of precursor evaporitic

lithology.

The carbonate interval downhole from 2702 m to 2906 m recovered no age

indications; since it was overlaid a thick volcanic interval (base of borehole at 3332 m

depth; at least 426 m thick of volcanic section), this part was attributed to the post

volcanic Nirim formation carbonate platform and to the early Jurassic in age. The

abandons of the infauna valvulinids (Fig. 9, 1-4) in the post volcanic carbonate

platform is indicating relatively harsh eutrophic conditions deep in the sediments

(anoxia? following Fugagnoli, 2004), and the epifauna glomospirids point to

oxic/dysoxic sediment/water interface but both are not age indications. The

involutinids (Aulotortus type, Fig. 9, 7-8) due their badly preservation, do not

contribute to age determination but the bad preserved probably Triasina species with

some remains of pillars on top left (Fig. 9, 10) indicates Norian-Rheatian age to the

interval. The occurrence of Orbitopsella sp. at 2799 m depth is attributed to caving,

and its first occurrence should be with the increasing variety of the Jurassic species at

2700 m depth. The occurrence of the Triasina might be controversial due its

preservation if it not reinforced by the upper part 200.9 M.Y (Rhaetian) radiometric

age of the underlain volcanic phase (Fig. 10; age from Golan, pers. Comm.).

24

Figure 10: Foraminifera recovered from interval 2199-3002 m in Elijah 3 borehole. 1- 4 - Valvulina

sp., sample 2810. 5-6 - Orbitopsella praecursor (Jurassic), sample 2699. 7-8 – Aulotortus sp., sample

2828. 9. “Siphovalvulina” sp., sample 2903. 10. Triasina? Sp., sample 2864.

4.2b Algal-mats and ooids facies in the post volcanic platform in

Elijha 3 borehole.

Fig. 10 shows a composite log of the interval and typical base of Nirim Fm.

Radiometric age provided by Golan (pers. Comm.). The 40 m at the base of the post-

volcanic carbonate have late Triassic foraminifers associated with species that can be

related to the Triassic and to the Jurassic as well (the valvulinids and the

glomospirids). The sedimentary components displaying a transition from brecciated

dolomites affected by volcanic fluids (Fig. 10) to shallow platform alternate between

energetic ooid environments to algal bounding associated with Taumathoporella sp.

F

igure

11

: L

og E

lija

h 3

: li

tho

log

y,

Sed

imen

tary

co

mp

onents

, fo

ram

inif

era,

sub

div

isio

n t

o a

ge-

stag

e and

87S

r/86S

r ra

tio

in 6

5 s

am

ple

s o

f 2

92

5 -

27

00

m i

nte

rval

4.2c The 87

Sr/86

Sr ratio

For this borehole 72 samples were analyzed for Sr isotopic composition and ca. 60%

for elemental chemistry (Table 1, Appendix). The results of the elemental analyses

indicate that the dominant mineral in the dissolved sample range widely from pure

dolomite (1% CaCO3) to ca. to near pure calcite (97%CaCO3). No correlation was

found between the calculated %CaCO3 and the 87

Sr/86Sr ratio. In addition, no

correlation was found between one of the major constitutes of the dissolve sample

(i.e. Ca, Mg, 1/Sr) and the 87

Sr/86

Sr ratio, which suggests no mixing of phases (i.e.

calcite with dolomite). Finally, a minor release of Al-Si and Fe-Mn is observed

suggesting some contribution if any of these phase during dissolution and possibly to

the Sr isotopic composition. Nevertheless, the 87

Sr/86

Sr ratio increase systematically

with depth from 2700 m to 2866 m below surface. Below 2866 m the ratio decreases

systematically (Fig. 12A).

Basalt sample taken from basket related to depth 2900-3000 m depth of the volcanic

interval was analyzed for Sr isotopic composition and concentration. The results are

87Sr/

86Sr = 0.70532 and 202 ppm Sr. Fig. 10A shows a significant constant decline of

the ratio values between 2840 m to 2700 m depth, and two groups of values deviate

out of the curve. Fig. 10B show the results projected on McArthur global curve.

Figure 12: Elijh Borehole, Sr87

/Sr86 ratio versus depth. Blue symbols represent samples with age

calculation while in red symbols are for excluded samples.

y = 2E-06x + 0.7019 R² = 0.9045

0.7071

0.7072

0.7073

0.7074

0.7075

0.7076

0.7077

0.7078

2650 2700 2750 2800 2850 2900 2950

87

Sr/8

6Sr

Depth m

Fig

ure

13

: T

he

87S

r/8

6S

r ra

tio

of

27

00

-29

50

m d

epth

inte

rval

in E

lija

h 3

bo

reho

le.

A.

The

iso

top

es r

atio

dis

trib

uti

on i

n t

he

stud

ied

inte

rval

. B

. T

he

bo

reho

le’s

iso

top

es r

atio

pro

ject

ed o

n t

he

glo

bal

87S

r/8

6S

r ra

tio

curv

e o

f M

cA

rthur

et a

l.,

20

12

. N

ote

that

the

curv

es

do

no

t en

tire

ly f

it d

ue

the

dif

fere

nt

X a

xis

val

ues

(yea

rs v

ersus

met

ers)

. E

ach d

ot

sho

uld

be

pro

ject

ed f

oll

ow

ing h

er v

alue

on t

he

curv

e to

def

ine

the

age

of

its

dep

th.

4.3 GA’ASH 2 BOREHOLE

4.3a Cathodoluminescence (CL)

No volcanic sequence was found in the borehole and indeed the general CL of the

borehole material appeared dull (DCL). The large dolomite crystals at 4422 m depth

(Fig. 12, 1-2) display DCL without and overprint of hydrothermal fluids. Only one

sample, at a depth of 4451 m (Fig. 12, 3-6) showed cementation with large Ca-rich

concentric zoned dolomite exhibiting differences in luminescence intensity. This

sample indicates hydrothermal activity that filled the sediment cavities and fractures.

4.3b Biostratigraphy

The studied interval with the T-J transition in Ga’ash 2 borehole is illustrated in Fig.

11 following lithology, sedimentary components, deposition environments and the

distribution of foraminifers’ species as recorded. Previous studies suggested that the

expected T-J transition should be posited in the interval 4562 – 4300 m depth. Hence

this interval was restudied in details by new thin sections. The disappearance of

Aulotortus friedli and A. sinuosus filled by the continued occurrence of the Late

Triassic species Aulutortus tumidus associated with valvuliniids, tetrataxis and

Turrispirilina sp. indicating the continue of Triassic species in relatively strained

conditions (Valvulininae, Tetrataxidae), before the occurrence of typical Jurassic

species (Litosepta sp.). Hence, the T-J transition should be shifted from the clayey

horizon

29

Figure 14: CL of 4422 – 4451 m samples in T-J transition interval at Ga’ash 2 borehole. 1. Few phases

of dolomitization, small crystal in sediment, large in caves, were 2., very dull luminescent (DCL; 4422

m depth). 3, Crystal growth on bioclastic sediment displays very bright luminescence (BCL) at 4., the

sediment itself and with sharp differences in luminescence intensity of the large crystals (4451 m

depth). 5. Same depth as above, with similar phenomenon.

Fig

ure

15

: C

om

po

site

lo

g o

f in

terv

al 5

03

0-

43

00

m d

epth

s in

Ga’a

sh 2

bo

reho

le. T

rias

sic

fora

min

ifer

s up

to

46

00

m a

fter

Ko

rngre

en a

nd

Ben

jam

ini,

20

06

; Ju

rass

ic f

ora

ms

1 a

fter

Buchb

ind

er a

nd

Sho

mro

ny

, 1

98

8;

mix

ass

em

bla

ge

of

fora

min

ifera

occ

urs

abo

ve

Mis

h’h

or

(?)

Fo

rmat

ion

(4

560

- 4

34

0 m

inte

rval)

, th

at c

an b

e as

signed

to

the

Lat

e T

rias

sic.

4.3c The 87

Sr/86

Sr ratio

For this borehole, 44 samples were dissolved and analyzed for elemental chemistry.

Amongst these samples 50 samples were analyzed for Sr isotopic composition (Table

2, Appendix). The results of the elemental analyses indicate that the dominant

minerals in the dissolved sample are down to 4577 m is dolomite (less than 10%

CaCO3) and below is calcite (>90%). This change is very abrupt. No correlation was

found between the calculated %CaCO3 and the 87

Sr/86

Sr ratio. In addition, no

correlation was found between one of the major constitutes of the dissolve sample

(i.e. Ca, Mg, 1/Sr) and the 87

Sr/86

Sr ratio, which suggests no mixing of phases (i.e.

calcite with dolomite). Finally, no significant release of Al-Si and Fe-Mn is observed.

The 87

Sr/86

Sr ratio increase systematically with depth (Fig. 16).As be seen two parallel

linear lines describe the sample. This could either represent small section duplication

or step out of the drilling.

Figure 16: Ga’ash Borehole, Sr87

/Sr86

ratio versus depth. Two set of samples can be seen; blue and

green symbols. The both have the same slope and initial.

y = 3E-06x + 0.6995 R² = 0.9221

y = 3E-06x + 0.7001 R² = 0.7213

0.7073

0.7073

0.7074

0.7074

0.7075

0.7075

0.7076

0.7076

0.7077

0.7077

0.7078

2650 2700 2750 2800 2850 2900 2950

87

Sr/8

6Sr

Depth m

32

Figure 17: The

87Sr/

86Sr ratio of 4400-4600 m depth interval in Ga’ash 2 borehole. The borehole’s

isotopes ratio projected on the global 87

Sr/86

Sr ratio curve of McArthur et al., 2012.

Figure 18: Facies of the Triassic – Jurassic transition in Elijah 3 and Ga’ash 2 boreholes: 1. Well sorted

ooid grainstone; Elijah 3 borehole, sample 2801 m depth.2. Algal mats associate with valvulininae (V)

and the algal species Thaumathoporella (Th), inner ramp; Elijah 3 borehole, sample 2810 m depth. 3.

Chaetid sponge (Sphinctozoan) polygonal morphology (appear also at 2822 and 2846, 2849, 2855 m

depths and filled with crude oil at 2873); Elijah 3 borehole, sample 2813 m depth. 4. Mixing of

moderate sorted normal ooids and peloids bounded by algae; Elijah 3 borehole, sample 2831 m depth

(appear also at 2858 m depth). 5. Algal mats associate with valvulininae (V), inner ramp; Ga’ash 2

borehole, sample 4428 m depth.6. Carbonate sand near dasyclad green algae (D) bioherm; the sand

with large pores indicating semi restricted part of marine barrier, under wave action of the innermost

platform. Ga’ash 2 borehole, sample 4482 m depth. 7. Aggregate grain carbonate (grapestone) bounded

by algae; seaward face of marine lagoon in wave action zone, in the photic zone. Ga’ash 2 borehole,

sample 4541 m depth; filled with crude oil at 4547 m depth. 8. Radial-fibrous concentric ooid

grainstone, relatively low energy shallow marine environment. Ga’ash 2 borehole, sample 4621 m

depth.

33

34

5. DISCUSSION

5.1 ASSINIGING NUMERICAL AGE TO THE BOREHOLES

In this study, we sought to apply Sr stratigraphy on samples taken from boreholes as

appose to exposed succession. In addition, because of the absence of fauna we could

only apply this method to bulk rock. The problems arise from working with cuttings

are two: (1) relative poor resolution which is inherent in cutting recovery. In the

studied boreholes the intervals were 3m (2) perturbations such as changing bits and

change in the rate of pumping can cause caving, material loss and drifting material to

higher levels.

Nevertheless, the studied intervals in the above boreholes are the best for the purposed

aim of this study i.e. understanding the T-J transition.

The problems in recovering relatable material from the boreholes as stated above were

taken into consideration when assigning numerical age to the measured 87

Sr/86

Sr ratio.

In addition the following was also taken into considerations: One of the three

boreholes, Ga’ash 2 show continues section along the T-J transition and has no

volcanics while the other two include volcanics between the Triassic and Jurassic

carbonate sequence. In addition, Elijah borehole is fresh borehole which preserved the

original material.

As indicated in the above results the method used indeed dissolved the CaCO3 with

no significant contribution from clay. This suggests that the measured 87

Sr/86

Sr ratio is

accurate and representative. However, many of the studied samples do not fall on the

curve of 87

Sr/86

Sr ratio change with time. This could be explained either as

perturbations or presence of volcanic sequence.

After confirming that the dominant contributor of Sr is CaCO3, using elemental

analysis, the measured 87

Sr/86

Sr ratio was compared to the sea water curve which

displays the change of the 87

Sr/86

Sr ratio with time (LOWESS, 3.3). Since samples

represent 3 m interval, the running average of 2 was calculated. Intervals which show

a distinct deviation from the expected evolution line of 87

Sr/86

Sr ratio with time were

removed and are discussed in details below.

Asher-Atlit 1: The analyzed intervals show no systematic with depth and the data

points are scattered. This is probably caused by the documented bit changes every 50

m and the fishing of drilling instruments. The possible contribution of Sr by volcanic

activity should also be considered. The measured 87

Sr/86

Sr ratio of the basalt from

35

Elija is 0.70532 with 202 ppm Sr. Any mixture should bring down the expected

values however there is no correlation between 1/Sr and the 87

Sr/86

Sr ratio (no

mixture) which may be a result of a similar Sr concentrations of the two components

(basalt and CaCO3; ca. 200 ppm). The presence of Anhydrite in the dissolved

solutions may explain the heterogeneous values and the high 87

Sr/86

Sr ratio. However,

up to date the Late Triassic sections was considered to be absent of evaporites,

although is well know from other Late Triassic sections in Eastern part of Israel

(Mohila Fm., Devora 2a, and in the Negev outcrops). To conclude a more specific

work is need in which the anhydrite must be removed prior to analyzing the 87

Sr/86

Sr

ratio.

Ga’ash 2: The chemistry of the analyzed samples indicates that the rock is dolomite

down to ~4577 m (~10% CaCO3) but below is calcite (80-90% CaCO3).

In this borehole there are many successive results which can indicate the age of the

section (Fig.17). The large interval of ca. 100 m (4440-4560) indicate a narrow range

of ages 194-196.5 Ma well suited to the Jurassic time. The calculated rate of

deposition is quite average, some 60 m per million years compare to 10-100 m per

million year (in tropical carbonate systems; summarized by Scholle et al., 1983). The

87Sr/

86Sr ratios below 4560 m vary but generally high. These ratios indicate ages of

between 200 to 204 Ma. If indeed these results are reliable, then the stratigraphic gap

is as large as 7 Ma. In order to confirm this section below must be further

investigated.

Elijah 3: The chemistry of the analyzed samples indicates that section becomes more

dolomite toward the surface. Some of the samples indicate high content of Mn (2903-

2921 m) which agreed with the stratigraphic position above and within volcanics. In

this borehole there are many successive results which can indicate the age of the

section (Fig.19). The large interval of ca. 150 m (2700-2850m depth) indicate a

narrow range of ages 187-198 Ma well suited to the Jurassic time. Again, the

calculated rate of deposition, some 14 m per million years is with agreement with the

known rates. The 87

Sr/86

Sr ratios below 2850 m vary but generally low. These results

may be attributed to the volcanic activity which should reduce the Sr isotope ratio

toward 87

Sr/86

Sr = 0.7054 of basalt. These ratios indicate ages of between 200 to 204

Ma.

It can be concluded that applying Sr stratigraphy can be done on boreholes but extra

care should be taken when calculating the age.

36

5.2 THE T-J TRANSITION BIOSTRATIGRAPHY

In general, the studied intervals are relatively poor in fauna remains and also are badly

preserved. Biostratigraphy recovered from the three intervals studied allowed to

define the Triassic and the Jurassic sections however, the boundary between the two

could have not determined because of lack of fauna remain (barren dolomite, base

Nirim Fm.).

In Asher-Atlit borehole Norian-Rhaetian reefs were discovered in two carbonate

break intervals within the volcanic sequence. This indicates that at least up to 5170,

the section is Triassic, contrary to previous work (Sherman, 1983) that determined the

T-J transition in this borehole is at depth of 5397 m. Indeed, Katzir et al., (2015)

reported a Norian age (205 Ma, volcanics) at 4840 m depth, some 5Ma prior to the T-

J boundary. Hence the section above should be further investigated.

The Triassic section in the Ga’ash borehole is topped by clayey horizon ascribed to

Mish’hor formation by Gerry and Derin (1981) claiming to mark the Triassic-Jurassic

transition. Hence, the 908 m thick Triassic section, interval 4600–5508 m in the

borehole, was assigned to Middle-Late Triassic using palynomorphs (Cousminer,

1981) and foraminifera (Korngreen and Benjamini, 2006). The immediate overlaid

dolomitic interval (4562 – 4335 m depth) above the clayey horizon was assigned to

the lower part of Nirim Formation, considered Jurassic in age, where Orbitopsella

praecursor zone lower appearance is at 4335 m depth (Buchbinder and Shomrony,

1988), 227 m above the base of the Formation.

However, in this study, foraminifera of Late Triassic were found above 4590 m

changing gradually to cosmopolitan foraminifera species that can related either to

Triassic or to Jurassic times.

The biostratigraphy of Elijah borehole was first published in Korngreen et al., (2010)

and in the current study the section above the volcanics was studied and Late Triassic

foraminifera were recovered up to 2850 m. In addition, at depth of 2700 m typical

Jurassic foraminifera were recovered. Hence the T-J transition should be between

2850 and 2700 m.

Based on the biostratigraphy it can be concluded that the T-J boundary is up well than

previously thought and probably should positioned at the lower part of the Nirim Fm.

37

5.3 FACIES RECORDED IN THE LATE TRIASSIC TO EARLY JURASSIC, NORTHERN COASTAL PLAIN OF ISRAEL

The Late Triassic reefal carbonates occur in Asher Atlit 1 borehole in the carbonate

breaks of the continuum volcanic eruptions at two intervals: one (5400 – 5550 m

depth) known from previous works and in higher interval (5180 – 5250 m depth). The

deepest one is 150 m thick and includes volcanic horizons and the other is 70 m thick

and composes of carbonate only. Both reefal intervals contain abundant calcified

sponges, typical to the Norian- Rhaetian reef structure known from the western

margins of the Tethys (Northern calcareous Alps and the West Carpathians; Flügel

1981, 1982), from the southern margins of the Tethys and as from the Late Triassic

margins faced the Panthalassa ocean too (Senowbari-Daryan et al., 2015).

Characteristically, the reefs carbonate are buildup structures containing infinite

number of voids, caves and pores in all sizes from micron to meter scales. These

voids can compose up to 80% of the structure and can later filled with carbonate

cement as can be seen in Figure 6. These fillings can alter the 87

Sr/86

Sr isotopic

signature of the sample. In the current case, volcanic eruption or related hydrothermal

activity probably changed the water isotope signal in the proximity environment, and

thus the sample values of Asher-Atalit. Similarly, this could be the explanation for the

reduced values in the Elijah borehole. Below 2860 m depth values are lower than

expected. Indeed, the volcanics in borehole appear just tens meters below. In both

boreholes (Asher-Atlit and Elijah) the exotic luminescence under the CL is associated

with corporation of active ions such as Mn, Pb and U (not studied in this work). Both

effects are attributed to the involved volcanic fluids and hence were named “the

volcanic effect”.

The end-Triassic event which devastated corals and reefs caused their absent 4-10 Ma

(Hettangian-Early Sinemurian stages of the Early Jurassic; Stanley, 1988; Kiessling et

al., 1999; Leinfelder et al., 2002). Hence the occurrence of Sphinctozoan (Fig. 13/3)

which is assign to a reefal environment indicates that this part of the section is of Late

Triassic age. The Sr stratigraphic age is ca. 198 to 202 Ma which is close enough to

the T-J transition.

In contrary to the above boreholes, in the Late Triassic interval of Ga’ash 2 borehole

no evidences of reefal structures were observed. Instead, the Late Triassic carbonate

interval is abruptly broken by clayey horizon (4555 – 4580 m depth), absent any

recovered fauna; the interval was assigned to Mish’hor Fm. It’s stratigraphic position,

38

the high probability of small interval of Triassic fauna continue above it and the

apparently ages gap between the Sr ratio (at 4532 m depth of 197.1 Ma) and the

faunal indication below it, positioned it parallel to volcanic activity, that may cause

the carbonate factory break down (acidification?). The absence of reef components

in Ga’ash 2 (as from other known Late Triassic sections from the Negev and central

Israel) further affirms that the regional Late Triassic reefal structures are tightly

connected to spatial distribution of the volcanism which elevated the sea floor,

increased nutrients accessibility etc.). Following the CL pattern, each colonization

occurred at ceasing of the activity, and the filling cement recorded the volcanic

influence.

During the Late Triassic transitioned into the Jurassic both the Elijah 3 and Ga’ash 2

boreholes display similar deposition environments of relatively proximal carbonate

environment composed of algal mats and ooids (Fig. 13, 1-8). Indeed, the occurrence

of Dacycladacean, Valvulininae, mollusks and other foraminifera is associated with

the microbial facies proceeding the T-J transition in Ga’ash 2 borehole (Fig. 11, up to

4700 m depth and Fig. 13,7), followed by interval of microbialic mats associated with

radial-fibrous concentric ooid grainstone (Fig. 11 and Fig. 13,8). During the T-J

transition the depositional environment had changed to Thaumathoporella and

dacycladacean algal mats that were absent the ooid component (Fig. 13/6). In Elijah 3

borehole (Fig. 9), the mixed radial-fibrous concentric ooids (Fig. 13,1,4) appears

immediately post the volcanic phase, within the algal mats environment (Fig. 13,2,5),

and hence may correlate with the middle zone of Ga’ash 2 in the T-J transition. Hence

the T-J transition as recorded in both Elijah 3 and Ga’ash 2 boreholes, in this work

indicate typical deposition environment of shallow carbonate environment dominant

by microbial facies, similar to the extensive stromatolitic limestones of the Late

Triassic of the Alps (Mancinelli et al., 2005) which and highly characterizes the entire

inner shelfs of the Tethys (Ritterbush et al., 2015).

The associated foraminifera assemblage is indicating high supply of organic matter to

the sediment and relatively low availability of oxygen (following Fugagnoli, 2004).

These restricted lagoonal-like conditions on a carbonate platform had been continued

into the Jurassic, characterized by biomicritic limestones containing the algae

Thaumatoporella sp. and ostracods, similar to many T-J transition’s sites of the Alps

(see Mancinelli et al., 2005).

39

The absence of noticeable sedimentary change in the transition suggests that the

sedimentary environment was stable and the eutrophic conditions continued from the

late Triassic and at least into the Sinemurian, until the occurrence of much richer

assemblage of foraminifera including the first appearance of the species Orbitopsella

(indicated in Elijah 3 and Ga’ash 2 boreholes).

5.4 PANGEA RIFTING AND THE REEFAL FACIES.

The age of the volcanism is essential in understanding the rifting and break-up of

Pangaea in our region. The accepted understanding is that rifting begun during the

Late Permian to Early Triassic and continued and intensified at the beginning of the

Norian (Ziegler, 1982, 1988; Veevers, 1994; Withjack et al., 1998; Golonka and Ford,

2000; Golonka, 2002; Veevers, 2004). During the Early and Middle Jurassic, the

North America and Gondwana begun separating, opening the Atlantic Ocean,

(Golonka and Ford, 2000; Golonka, 2002; Ford and Golonka, 2003). Some studies

suggest that the opening of Alpine Tethys was concurrently (Golonka, 2004) which

was forced by mantle plume activity (following Marzoli et al., 1999; Golonka and

Bocharova, 2000; Marzoli et al., 2004). The northwestern Neotethys region consisted

of numerous horst blocks capped by carbonate platforms and reefs with adjacent

grabens filled with deeper-water black mudstone and organic-rich shale facies. These

tensional structures were essentially non volcanic (Ziegler, 1982).

Since the 35 meters above the base of the volcanic-free carbonate sequence (base

Nirim formation), that overlaid the mixed volcanic/carbonate succession in Elijah 3,

yield Sr ratio age of 198-202 Ma, the volcanic succession bellow is found to be of

Triassic age, and no late volcanic phases were recorded in the borehole (Korngreen et

al., 2010). This study indicates that the volcanism at least in Elijah 3, is of Late

Triassic age older than previously suggested.

The volcanics preceded the T-J transition, and the transition itself, following the

spatially distributions of shallow water environments, occurred specifically during

volcanic and tectonic quiescence (opposing claims of rifting phases; e.g. Garfunkel,

1989; Hirsch et al., 1998). The volcanic time-constrains, does not indicate oceanic-

like crust development (Ben-Avraham and Hall, 1977; Garfunkel and Derin, 1984;

Garfunkel, 1989) at least not in this location. The base of Nirim Formation that is

assigned here to the Hettangian, Sinemurian and the Pliensbachian, and not indicating

a sedimentary gap at the Early Jurassic (following Derin and Reiss, 1966; Derin,

40

1974) was probably deposited at a tectonic turning point, when the region changed

from active rifting to basin sagging. Apparently, the volcanics in Elijah 3 borehole is

coincident with the earliest pulses of the CAMP volcanism that precede the T–J

boundary (e.g. Marzoli et al., 2004; Cirilli et al., 2009; Deenen et al., 2010; Ruhl et

al., 2010, 2011; Schaller et al., 2011), bur this is all its participation in the Tethys and

the Atlantic opening.

This Late Triassic volcanic phase can explain the extirpation event of part of the

micro-fauna at the Late Triassic, but as well stimulated the occurrence of

sphinctozoan reefs.

Although the partially successful and unaccomplished study on the Sr isotopes ratio

and facies analyzes of the T-J in Asher Atlit 1 (Fig.5), the volcanics succession there

ends at the same depth as in Elijah 3 borehole (Fig. 9; 3000 m depth), which may

imply to a same geological history.

6. CONCLUSIONS

1. It can be concluded that applying Sr stratigraphy can be done on boreholes but

extra care should be taken when calculating the age.

2. In Elijah 3 borehole, a significant constant decline of the Sr ratio values between

2840 m to 2700 m depth, yielded early Jurassic ages and determined the T-J

transition positioned at ca. 2855 m depth, above the volcanics, and above the base

of Nirim Fm.

3. The volcanics in Elijah 3 were intruded prior to the Triassic-Jurassic transition

and coincident with the earliest pulses of the CAMP volcanism, however, no later

volcanic phases were recorded in the borehole.

4. In Ga’ash 2 borehole, similar significant results yield early Jurassic ages (197

Ma) at depth 4532, but the T-J transition couldn’t be identified.

5. Asher Atlit 1: This work shows that higher carbonate break of the volcanic

succession (the 5270 – 5180 m interval), is still Norian – Rhaetian in age and

represent reefal environment with Late Triassic components contemporary with

volcanic eruptions; together with the radioactive ages of about 205 M.Y., 550 m

above it (~ 4860 m depth, Fig. 5), indicates that the Norian-Rhaetian transition is

still up-hole; indicating with is no doubt, that the Triassic-Jurassic transition

should be far higher.

41

6. In Asher Atlit 1 the Sr stratigraphy failed to predict ages , and the assumption is

that it is a result of “Volcanic Effect”.the carbonate interval overlaid the volcanic

succession (interval 3000-2900 should be re-study in terms of Sr isotopes’

chronostratigraphy and facies interpretation to figure out the extent of similarity

with the carbonates overlaid the volcanics in Elijah 3 borehole.

7. The Late Triassic transitioned into the Jurassic ( Elijah 3 and Ga’ash 2 boreholes)

display similar and typical deposition environments of relatively proximal

carbonate environment composed of algal mats and ooids preceding, during and

post the transition; similar to the extensive stromatolitic limestones of the inner

shelfs of the Late Triassic of the Alps and the entire Tethyian shallow

environments.

8. Following the results in Elijah3 and Ga’ash 2 boreholes, the regional T-J

transition may considered as occurring simultaneously with volcanic and tectonic

quiescence; probably at the turning point from active rifting to sagging.

9. It is concluded that the base of Nirim Formation is assigned here to the

Hettangian, Sinemurian and the Pliensbachian, indicates no sedimentary gap at

the Early Jurassic.

10. The early Jurassic carbonates were probably deposited at a tectonic turning point.

11. The volcanics in Elijah 3 borehole is coincident with the earliest pulses of the

CAMP volcanism that preceded the T–J. However, no other activity is observed

related to the Tethys and the Atlantic opening.

12. This Late Triassic volcanic phase can explain the extirpation event of part of the

micro-fauna at the Late Triassic, but as well stimulated the occurrence of

sphinctozoan reefs.

43

REFERENCES

Ben‐Avraham, Z., Hall, J.K., 1977. Geophysical survey of Mount Carmel structure

and its extension into the eastern Mediterranean. Journal of Geophysical

Research, 82, 793-802.

Blackburn, T. J., Olsen, P. E., Bowring, S. A., McLean, N. M., Kent, D. V., Puffer, J.,

McHone, G., Rasbury. T.E., Et-Touhami, M., 2013. Zircon U-Pb geochronology

links the end-Triassic extinction with the Central Atlantic Magmatic

Province. Science, 340, 941-945.

Bosellini, A., Rossi, D., 1974. Triassic carbonate buildups of the Dolomites, northern

Italy, Special Publications of SEPM, Reef in time and space, 209-.

Buchbinder, B., Shomrony, A. 1988. Sedimentology, porosity development and

genetic subdivision of the lower Jurassic Nirim formation in the Ga’ash 2

borehole. Report GSI/4/88 (umpub.), 10 pp.

Buchbinder, B., le Roux, J.P., 1993. Inner platform cycles in the Ardon formation:

Lower Jurassic, southern Israel. Israel journal of earth-sciences, 42(1), 1-16.

Chablais, J., Martini, R., Kobayashi, F., Stampfli, G. M., Onoue, T., 2011. Upper

Triassic foraminifers from Panthalassan carbonate buildups of southwestern Japan

and their paleobiogeographic implications. Micropaleontology, 93-124.

Cirilli, S., Marzoli, A., Tanner, L., Bertrand, H., Buratti, N., Jourdan, F., Bellieni, G.,

Kontak, D., Renne, P.R., 2009. Latest Triassic onset of the Central Atlantic

Magmatic Province (CAMP) volcanism in the Fundy Basin (Nova Scotia): new

stratigraphic constraints. Earth and Planetary Science Letters 286, 514–525.

Cousminer, L.H., 1981. Palynostratigraphy, thermal alteration index and kerogen

characteristics of the Ga’ash 2 well sequence. State of Israel, ministry of energy

and Infrastructure, geological survey report P/2/81, 21 pp.

Cousminer, L.H., 1982. Palynology and TAI of samples from Atlit 1 well (cutting

from 5180-5240m), report submitted to Oil Exploration (Investments) LTD, 3 p.

Deenen, M.H.L., Ruhl, M., Bonis, N.R., Krijgsman, W., Kuerschner, W.M., van

Reitsma, M., Bergen, M.J., 2010. A new chronology for the end-Triassic mass

extinction. Earth and Planetary Science Letters 291, 113–125.

Derin, B., Reiss, Z., 1966. Jurassic microfacies of Israel, Israel Program for Sci.

Israel Ins. Petrol. Tel Aviv, Spec. Publ.

Derin, B., 1974. The Jurassic of central and northern Israel. Isr. Inst. Petrol. Rep.

Dvorkin, A., Kohn, B. P., 1989. The Asher Volcanics, northern Israel: petrography,

mineralogy, and alteration. Israel journal of earth-sciences, 38(2-4), 105-123.

Fugagnoli, A., 2004. Trophic regimes of benthic foraminiferal assemblages in Lower

Jurassic shallow water carbonates from northeastern Italy (Calcari Grigi, Trento

Platform, Venetian Prealps). Palaeogeography, Palaeoclimatology,

Palaeoecology, 205(1), 111-130.

Flügel, E., 2002. Triassic reef patterns. In: Phanerozoic Reef Patterns, SEPM Special

Publication No. 72, 391-463.

44

Galli, M. T., Jadoul, F., Bernasconi, S. M., & Weissert, H., 2005. Anomalies in global

carbon cycling and extinction at the Triassic/Jurassic boundary: evidence from a

marine C-isotope record. Palaeogeography, Palaeoclimatology,

Palaeoecology, 216, 203-214.

Garfunkel, Z., 1983. Examination of cuttings from Atlit 1 borehole (Appendix A, p.

67), in: Sherman, J. (1983), Completion report Asher Atlit 1 (Deepened), Energy

exploration, Huston, Texas.

Garfunkel, Z., Derin, B., 1984. Permian-early Mesozoic tectonism and continental

margin formation in Israel and its implications for the history of the Eastern

Mediterranean. Geological Society, London, Special Publications, 17(1), 187-201.

Garfunkel, Z., 1989. Tectonic setting of phaneroozoic magmatism in Israel. Israel

journal of earth-sciences, 38(2-4), 51-74.

Gerry, E., Derin, B., 1981. Late Permian-Late Triassic in Israel and its significance to

oil exploration, in: Symposium on Oil Exploration in Israel, Israel Geological

society abstract vol., 9-11.

Gerry, E., 1983. Upper Triassic microfauna & microfacies in Asher Atlit 1 (Appendix

B, p.68), in: Sherman, J. (1983), Completion report Asher Atlit 1 (Deepened),

Energy exploration, Huston, Texas.

Goldberg, M., 1964. The Arad Group (Jurassic) in the Northern Negev, Geol. Survey

report No. OD, 1, 64.

Goldbery, R., 1979. Sedimentology of the Lower Jurassic flint clay bearing Mishhor

Formation, Makhtesh Ramon, Israel. Sedimentology, 26(2), 229-251.

Goldbery, R., 1982. Palaeosols of the Lower Jurassic Mishhor and Ardon Formations

(‘Laterite Derivative Facies’), Makhtesh Ramon, Israel.Sedimentology, 29(5),

669-690.

Golonka, J., & Ford, D. (2000). Pangean (late Carboniferous–Middle Jurassic)

paleoenvironment and lithofacies. Palaeogeography, Palaeoclimatology,

Palaeoecology, 161(1), 1-34.

Golonka, J., Bocharova, N.Y., 2000. Hot spot activity and the break-up of

Pangea. Palaeogeography, Palaeoclimatology, Palaeoecology, 161(1), 49-69.

Golonka, J., 2004. Plate tectonic evolution of the southern margin of Eurasia in the

Mesozoic and Cenozoic. Tectonophysics, 381(1), 235-273.

Golonka, J., 2007. Late Triassic and Early Jurassic palaeogeography of the

world. Palaeogeography, Palaeoclimatology, Palaeoecology, 244(1), 297-307.

Gradstein, F.M., Ogg, J.G., Smith, A.G., 2004. A geologic time scale 2004 (Vol. 86).

Cambridge University Press.

Gvirtzman, G., Steinitz, G., 1983. The Asher volcanics—an early Jurassic event in

northern Israel. Israel Geological Survey Current Research, 1982, 28-33.

Gvirtzman, G., Teleman, E., Klang, A., 1984. Ga’ash-2, geological completion report.

Oil Exploration (Investments) LTD., report 84/33, 37 pp., 32 figs.

Ford, D., Golonka, J., 2003. Phanerozoic paleogeography, paleoenvironment and

lithofacies maps of the circum-Atlantic margins. Marine and Petroleum

Geology, 20, 249-285.

45

Frank, J.R., Carpenter, A.B., Oglesby, T.W., 1982. Cathodoluminescence and

composition of calcite cement in the Taum Sauk Limestone (Upper Cambrian),

southeast Missouri. Journal of Sedimentary Research, 52, 631-638.

Fu, X.G., Wang, J., Tan, F.W., Chen, M., & Chen, W. B., 2010. The Late Triassic

rift-related volcanic rocks from eastern Qiangtang, northern Tibet (China): age

and tectonic implications. Gondwana Research, 17, 135-144.

Heller‐Kallai, L., Nathan, Y., Zak, I., 1973. Clay mineralogy of Triassic sediments in

southern Israel and Sinai. Sedimentology, 20, 513-521. ,

Hirsch, F., Picard, L., 1988. The Jurassic facies in the Levant. Journal of Petroleum

Geology, 11, 277-308.

Hirsch, F., Bassoullet, J. P., Cariou, E., Conway, B., Feldman, H. R., Grossowicz, L.,

Honigstein, A., Owen, E.F., Rosenfeld, A., 1998. The Jurassic of the southern

Levant. Biostratigraphy, palaeogeography and cyclic events. Mémoires du

Muséum national d'histoire naturelle, 179, 213-235.

Holland, H. D., 1978. The Chemistry of the Atmosphere and Oceans: New York,

Wiley Interscience, The geologic history of seawater, in Elderfield, H., Volume

Editor, The Oceans and Marine, 351 p.

Katzir, Y., Golan, T., Coble, M., (2015). The timing of rifting-related magmatism in

the Levant margins: U-Pb dating of zircons from deep boreholes in the coastal

plain of Israel. Geophysical Research Abstracts, 17, EGU2015-4438, 2015.

Kiessling, W., Flügel, E., Golonka, J., 1999. Paleoreef maps: evaluation of a

comprehensive database on Phanerozoic reefs. AAPG bulletin, 83, 1552-1587.

Kohn, B.P., Lang, B., Steinitz, G., 1993. 40

Ar/39

Ar dating of the Atlit-1 volcanic

sequence, northern Israel. Israel Journal of Earth Sciences, 42, 17-28.

Korngreen, D., and Benjamini, C., 2001. Upper Triassic reef facies in the Asher-Atlit-

1 borehole, northern Israel: microfacies, cement stratigraphy and paleogeographic

implications. Facies, 45, 1-23.

Korngreen, D., and Benjamini, C., 2006. Foraminiferal assemblage-based

biostratigraphy and correlation of the Triassic of northern Israel. Israel Journal of

Earth Sciences, 55.

Korngreen, D., and Benjamini, C., 2010. The epicontinental subsiding margin of the

Triassic in northern Israel, north Arabian Plate. Sedimentary Geology, 228, 14-45.

Korngreen, D., and Benjamini, C., 2011, Platform to shelf edge transect, Triassic of

Northern Israel, North Arabian Plate. Sedimentary Geology, 236, 164–184.

Leinfelder, R.R., Schmid, U.D., Node, M., Werner, W., 2002. Jurassic reef patterns—

the expression of a changing globe. In: Phanerozoic Reef Patterns, SEPM Spec.

Pub. 72, 465-520.

Mancinelli, A., Chiocchini, M., Chiocchini, R. A., Romano, A., 2005.

Biostratigraphy of Upper Triassic-Lower Jurassic carbonate platform sediments of

the central-southern Apennines (Italy). Rivista Italiana di Paleontologia e

Stratigrafia, 111, 271-283.

Marzoli, A., Bertrand, H., Knight, K. B., Cirilli, S., Buratti, N., Vérati, C., Nomade,

S., Renne, R.P., Youbi, N., Martini, R., Allenbach, K., Neuwerth, R., Rapaille, C.,

46

Zaninetti, L., Bellieni, G., 2004. Synchrony of the Central Atlantic magmatic

province and the Triassic-Jurassic boundary climatic and biotic

crisis. Geology, 32, 973-976.

McArthur, J. M., Howarth, R. J., Shields, G.A., 2012. Strontium isotope

stratigraphy. The geologic time scale, 1, 127-144.

Mouty, M., 2000. The Jurassic in Syria: an overview. Lithostratigraphic and

biostratigraphic correlations with adjacent areas. Mémoires du Muséum national

d'histoire naturelle, 182, 159-168. Nevo 1963;

Olsen, P.E., Kent, D.V., Et-Touhami, M., Puffer, J., 2003. Cyclo-, magneto-, and bio-

stratigraphic constraints on the duration of the CAMP event and its relationship to

the Triassic-Jurassic boundary. The Central Atlantic Magmatic Province: Insights

from Fragments of Pangea, 7-32.

Pagel, M., Barbin, V., Blanc, P., Ohnenstetter, D., 2000. Cathodoluminescence in

geosciences: an introduction. InCathodoluminescence in Geosciences (pp. 1-21).

Springer Berlin Heidelberg.

Pálfy, J., 2003. Volcanism of the Central Atlantic Magmatic Province as a potential

driving force in the end-Triassic mass extinction. GEOPHYSICAL

MONOGRAPH-AMERICAN GEOPHYSICAL UNION, 136, 255-267.

Pierson, B.J., 1981. The control of cathodoluminescence in dolomite by iron and

manganese. Sedimentology, 28(5), 601-610.

Ruhl, M., Deenen, M.H.L., Abels, H.A., Bonis, N.R., Krijgsman, W., Kürschner,

W.M., 2010. Astronomical constraints on the duration of the early Jurassic

Hettangian stage and recovery rates following the end-Triassic mass extinction (St

Audrie's Bay/East Quantoxhead, UK). Earth and Planetary Science Letters 295,

262–276

Ruhl, M., Kürschner, W.M., 2011. Multiple phases of carbon cycle disturbance from

large igneous province formation at the Triassic–Jurassic transition. Geology 39,

431–434.

Richter, D.K., Zinkernagel, U., 1981. Zur Anwendung der Kathodolumineszenz in der

Karbonatpetrographie. Geologische Rundschau,70, 1276-1302.

Ritterbush, A.K., Ibarra, Y., Bottjer, D. J.,Corsetti, A.F.,Rosas, S.,Wesr, A.J.,

Berelson, M.W., Yager, A,J., 2015. Marine ecological-shifts following the

Triassic-Jurassic mass extinction. The Paleontological Society Papers, 21, 121-

136.

Robertson, A.H.F., 1993. Mesozoic–Tertiary sedimentary and tectonic evolution of

Neotethyan carbonate platforms, margins and small ocean basins in the Antalya

Complex of Southwest Turkey. Tectonic Controls and Signatures in Sedimentary

Successions, 415-465.

Searle, M.P., Graham, G.M., 1982. “Oman Exotics”—Oceanic carbonate build-ups

associated with the early stages of continental rifting. Geology, 10(1), 43-49.

Schaller, M.F., Wright, J.D., Kent, D.V., 2011. Atmospheric PCO2 perturbations

associated with the Central Atlantic Magmatic Province. Science 331, 1404–1409.

47

Sherman, J., 1983. Completion report Asher Atlit 1 (Deepened), Energy exploration,

Huston, Texas.

Schoene, B., Guex, J., Bartolini, A., Schaltegger, U., Blackburn, T.J., 2010.

Correlating the end-Triassic mass extinction and flood basalt volcanism at the 100

ka level. Geology, 38, 387-390.

Scholle, P.A., Arthur, P.A., Ekdal, A.A., 1983. Pelagic. In: Scholle, P.A., Bebout,

D.G., Moore, C.H. (Eds.), Carbonate Depositional Environments: AAPG Memoir

33, P. 640.

Senowbari-Daryan, B., Di Stefano, P., Abate, B., 2015. Hypercalcified sponges from

the upper Triassic reefs of Sicily, museo Geologico “G.G.Gemmallaro”, Univ.

Degli studi di Palermo, ISSN 1121-1415, 300 p.

Smalley, P. C., Higgins, A. C., Howarth, R. J., Nicholson, H., Jones, C. E.,

Swinburne, N. H. M., & Bessa, J. (1994). Seawater Sr isotope variations through

time: a procedure for constructing a reference curve to date and correlate marine

sedimentary rocks. Geology, 22(5), 431-434.

Stanley, G.D., 2003. The evolution of modern corals and their early history. Earth-

Science Reviews, 60, 195-225.

Veevers, J.J., 1994. Pangea: Evolution of a supercontinent and its consequences for

Earth’s paleoclimate and sedimentary environments. Geological Society of

America Special Papers, 288, 13-24.

Veevers, J.J. 2004. Gondwanaland from 650–500 Ma assembly through 320 Ma

merger in Pangea to 185–100 Ma breakup: supercontinental tectonics via

stratigraphy and radiometric dating. Earth-Science Reviews, 68, 1-132.

Whiteside, J.H., Olsen, P.E., Kent, D.V., Fowell, S.J., Et-Touhami, M., 2007.

Synchrony between the Central Atlantic magmatic province and the Triassic–

Jurassic mass-extinction event? Palaeogeography, Palaeoclimatology,

Palaeoecology, 244, 345-367.

Whiteside, J.H., Olsen, P.E., Eglinton, T., Brookfield, M.E., Sambrotto, R.N., 2010.

Compound-specific carbon isotopes from Earth’s largest flood basalt eruptions

directly linked to the end-Triassic mass extinction. Proceedings of the National

Academy of Sciences, 107, 6721-6725.

Withjack, M.O., Schlische, R.W., Olsen, P.E., 1998. Diachronous rifting, drifting, and

inversion on the passive margin of central eastern North America: an analog for

other passive margins. AAPG bulletin, 82, 817-835.

Ziegler, P.A., 1982. Triassic rifts and facies patterns in Western and Central

Europe. Geologische Rundschau, 71(3), 747-772.

Ziegler, P.A., 1988. Post-Hercynian plate reorganization in the Tethys and Arctic-

North Atlantic domains. Triassic-Jurassic rifting: New York, Elsevier, 71.

AP

PE

ND

IX

Tab

le 1

: E

lem

enta

l co

mp

osi

tion (

mg/L

) an

d8

7S

r/86S

r ra

tio o

f A

sher

Atl

it 1

bore

hole

De

pth

m

8

7Sr

/86

Sr

Ca

Mg

Mn

N

a K

SO

4

Al

Fe

Ba

Sr

SiO

2

f C

aCO

3

54

45

0

.70

75

59

9

03

6

75

5

2

2

2

06

5

2

9

15

5

1

5

0.9

7

54

48

0

.70

76

49

3

35

10

3

16

1

7

19

3

7

91

1

7

10

4

34

1

6

19

0

.97

54

51

0

.70

76

13

1

69

04

2

22

9

6

4

3

92

1

6

81

2

2

9

29

0

.95

54

54

0

.70

74

74

2

81

42

3

89

1

3

8

-2

64

8

9

10

5

20

1

5

21

0

.95

54

57

0

.70

76

32

3

45

88

3

77

1

2

16

7

8

23

2

5

81

4

1

19

2

2

0.9

6

54

60

0

.70

72

37

2

82

50

1

49

4

23

1

3

5

64

5

11

6

08

1

6

15

2

0

0.8

4

54

69

0

.70

75

83

1

99

79

2

45

7

9

6

4

69

2

4

87

2

4

12

2

0

0.9

6

54

75

0

.70

74

52

54

78

0

.70

73

9

54

81

0

.70

82

26

2

59

51

2

74

7

1

0

5

64

1

27

6

4

70

2

0

32

0

.96

54

84

0

.70

77

85

4

46

80

5

94

9

2

5

7

10

74

2

8

81

3

7

30

1

7

0.9

5

54

87

0

.70

74

92

6

51

23

3

94

3

44

4

3

15

7

17

42

5

96

1

13

4

74

4

3

7

0.8

2

54

90

0

.70

81

27

1

49

11

2

39

5

1

9

4

35

6

21

6

0

33

1

1

31

0

.95

54

93

0

.70

72

6

25

92

1

19

8

9

6

-1

59

9

7

62

7

1

5

23

0

.97

54

96

0

.70

77

33

2

11

32

2

74

7

7

5

4

89

2

3

74

1

8

13

3

5

0.9

5

54

99

0

.70

78

46

1

50

96

1

43

3

7

2

3

38

9

1

9

16

9

2

9

0.9

7

55

08

0

.70

79

16

1

70

46

3

44

1

3

24

0

4

10

1

2

12

8

29

1

2

29

0

.93

55

11

0

.70

76

04

1

58

24

2

18

1

0

22

3

3

73

1

1

76

9

1

0

30

0

.95

55

23

10

39

2

12

5

4

6

8

25

9

35

3

3

24

8

3

2

0.9

6

48

55

26

0

.70

79

48

2

04

52

2

64

1

6

14

5

5

20

4

7

12

7

28

1

3

27

0

.95

55

28

55

33

0

.70

74

34

1

74

89

1

28

3

22

9

1

5

39

5

12

4

19

5

5

12

2

8

0.7

9

55

34

0

.70

80

49

6

89

19

1

11

9

40

4

3

5

16

95

4

8

44

7

56

3

5

1

0.9

4

55

40

0

.70

77

53

1

73

71

1

48

6

1

1

0

39

3

6

33

9

1

1

18

0

.97

55

43

0

.70

76

46

1

62

58

1

18

6

5

5

3

69

7

3

9

14

1

1

20

0

.97

55

52

0

.70

81

11

3

04

63

4

53

7

1

5

9

73

0

46

7

4

33

2

1

8

0.9

5

55

60

0

.70

79

07

1

20

36

1

33

3

2

1

4

27

9

11

2

1

9

8

27

0

.96

55

66

55

72

0

.70

76

32

1

20

26

7

9

18

8

2

2

73

6

2

1

23

7

2

0

0.9

7

55

75

0

.70

72

66

2

00

03

1

54

1

6

5

5

45

7

15

2

9

7

13

3

2

0.9

7

55

81

0

.70

82

92

1

15

36

1

22

1

9

17

8

2

74

4

0

46

2

6

8

27

0

.96

55

94

0

.70

74

48

2

10

69

1

62

3

0

4

2

49

0

11

1

9

4

13

2

8

0.9

7

55

97

0

.70

77

06

1

12

33

1

45

2

9

6

3

26

7

82

6

9

16

7

2

0

0.9

5

49

Tab

le 2

: E

lem

enta

l co

mposi

tion (

mg/L

) an

d8

7S

r/86S

r ra

tio o

f E

lija

h 3

bore

hole

Dep

th

m

87S

r /8

6S

r

Ca

M

g

Mn

N

a

K

SO

4

Al

Fe

Ba

Sr

SiO

2

f C

aC

O3

Ass

. A

ge

±0

.75 M

a

27

00

0.7

072

7

27

03

0.7

073

0

18

8.4

27

06

0.7

073

4

18

9.1

27

09

0.7

073

2

18

9.3

27

12

0.7

073

2

18

9.0

27

15

0.7

073

0

18

8.9

27

18

0.7

073

0

18

8.7

27

21

0.7

073

6

18

9.2

27

24

0.7

073

4

18

9.6

27

27

0.7

073

7

18

9.7

27

30

0.7

074

3

19

0.4

27

33

0.7

073

9

19

0.5

27

36

0.7

074

3

27

39

0.7

073

8

19

0.1

27

42

0.7

074

1

27

45

0.7

073

5

27

48

0.7

073

3

18

9.4

27

51

0.7

073

5

18

9.4

27

54

0.7

073

3

18

9.5

27

57

0.7

073

8

18

9.6

27

60

0.7

073

7

27

66

0.7

073

5

18

9.8

27

69

0.7

073

8

18

9.9

27

72

0.7

074

3

19

0.9

50

27

75

0.7

073

8

19

0.5

27

78

0.7

074

3

19

0.5

27

81

0.7

073

1

27

84

0.7

072

1

27

87

0.7

072

8

27

90

0.7

072

1

27

93

0.7

071

4

27

96

0.7

073

3

28

00

0.7

073

1

28

01

0.7

075

1

14

014

59

27

5.0

13

0

11

08

3.9

8

.1

24

.0

1.1

1

94

.2

28

04

0.7

074

4

42

880

45

34

4.6

15

5

61

4.7

5

8.6

1

4.9

8

.8

19

1.3

28

10

0.7

074

9

28

054

58

18

4.0

34

1

63

3.3

4

7.4

1

8.1

4

.6

19

1.4

28

13

0.7

075

5

22

127

13

241

7.2

24

3

21

7

1.9

6

.4

16

.3

0.1

1

96

.6

28

16

0.7

075

7

22

550

10

375

5.4

72

5

12

7

3.6

2

1.1

1

2.3

1

.4

19

6.2

28

19

0.7

075

5

18

691

10

675

5.5

2

8.8

1

5.5

4

67

65

87

3.6

6

.8

20

.9

0.3

1

95

.9

28

22

0.7

075

0

17

268

88

68

4.9

4

8.6

7

1.0

6

36

21

5

94

3.4

1

4.9

2

1.4

0

.7

19

4.5

28

25

0.7

075

3

16

365

89

62

5.4

3

7.8

9

6.8

4

88

24

8

13

5

3.1

1

2.9

1

7.0

0

.4

19

6.2

28

28

0.7

075

4

11

095

56

91

3.8

3

5.2

1

37

.3

36

8

34

1

93

1.8

1

1.5

2

9.6

0

.4

19

4.4

28

31

0.7

075

9

23

230

12

793

9.2

6

2.8

2

92

.8

72

5

79

2

28

0

5.8

2

1.4

2

0.0

0

.5

19

7.0

28

34

0.7

075

8

16

591

92

06

6.7

4

4.1

1

02

.3

53

8

29

1

14

4

2.0

1

0.9

9

.3

0.4

1

97

.5

28

37

0.7

075

8

44

102

45

37

4.6

1

5.9

5

0.7

1

06

5

14

1

55

4.4

5

7.8

1

8.7

9

.1

19

6.6

28

40

0.7

075

2

35

787

19

875

13

.0

10

7.4

1

00

.3

17

99

26

3

35

4

2.5

2

7.4

1

1.8

0

.8

19

5.7

28

43

0.7

076

3

17

952

96

25

6.9

5

4.3

2

00

.1

70

3

56

4

24

5

4.4

2

4.4

2

2.1

0

.5

19

7.6

28

46

0.7

075

8

14

865

78

13

6.1

4

6.1

2

09

.8

54

2

45

8

15

4

2.9

1

2.2

2

4.8

0

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19

6.5

28

49

0.7

075

8

12

775

66

55

5.9

2

9.9

7

5.2

9

42

22

5

26

9

1.4

1

0.6

2

7.8

0

.4

19

6.6

28

52

0.7

075

6

12

366

67

19

5.6

2

6.8

7

7.0

4

85

24

9

13

5

1.8

9

.3

27

.0

0.3

1

96

.2

28

55

0.7

077

6

19

460

10

948

15

.4

55

.1

18

8.1

7

97

61

1

34

6

8.4

1

1.4

1

6.3

0

.4

20

2.1

51

28

58

0.7

076

7

12

816

63

24

11

.3

42

.0

12

3.5

7

98

40

7

26

0

6.5

1

0.4

3

0.7

0

.6

19

7.6

28

64

0.7

077

0

17

300

91

15

18

.7

61

.3

19

4.3

9

52

71

5

35

5

15

.7

18

.9

17

.2

0.6

2

03

.2

28

66

0.7

075

7

32

868

46

61

3.8

2

5.2

4

0.5

9

35

11

7

55

0.3

1

4.5

1

6.5

6

.3

28

69

0.7

073

4

33

112

44

6

1.0

8

.3

3.1

8

21

18

8

0.1

1

1.9

2

0.8

8

.1

28

72

0.7

074

3

14

551

35

8

0.6

1

4.1

5

.9

35

5

18

11

0.1

6

.4

33

.3

3.5

28

75

0.7

073

9

32

733

51

10

3.9

3

0.1

6

8.6

1

04

3

18

5

96

0.3

2

5.8

1

7.6

6

.1

28

78

0.7

073

6

31

263

22

37

6.9

1

1.8

2

2.9

8

78

10

0

81

0.2

1

5.4

1

9.5

6

.9

28

81

0.7

073

0

15

513

18

30

4.5

9

.7

7.1

4

09

36

60

0.2

8

.2

31

.4

3.1

28

84

0.7

071

4

18

572

35

99

5.9

1

0.7

1

6.9

4

90

58

64

0.2

9

.7

34

.1

3.2

28

87

0.7

073

3

30

263

28

32

5.2

1

9.8

8

4.3

9

70

25

1

13

6

0.3

1

5.9

1

8.7

6

.4

28

90

0.7

072

9

37

203

36

6

0.7

1

2.2

6

.4

95

0

35

13

0.2

1

9.3

1

8.0

9

.1

28

93

0.7

072

2

27

386

30

0

2.4

3

0.8

1

4.1

6

89

23

5

11

9

0.3

1

3.5

1

7.0

6

.7

28

96

0.7

070

7

15

200

39

96

67

.7

11

.6

25

.4

43

6

92

21

9

0.2

8

.5

28

.4

2.2

29

00

0.7

073

7

20

364

10

692

13

6.7

4

0.1

6

6.7

6

10

17

7

48

3

0.4

2

0.5

1

8.7

0

.7

29

03

0.7

073

9

13

574

31

60

48

.9

11

.1

24

.6

38

4

78

21

3

0.2

9

.4

29

.3

2.1

29

06

0.7

072

6

31

579

65

24

31

.9

34

.9

86

.2

88

8

32

3

39

9

0.6

2

9.4

2

1.8

5

.2

29

09

0.7

072

5

23

457

46

6

14

.0

14

.1

42

.3

63

3

17

0

20

3

0.3

1

9.8

3

2.0

5

.7

29

12

0.7

072

8

33

412

48

9

3.3

1

2.6

5

3.4

8

36

15

9

80

0.3

1

5.7

2

0.9

8

.1

29

15

0.7

073

3

21

753

16

88

5.1

9

.4

4.4

5

46

21

23

0.2

1

2.4

2

8.5

4

.7

29

18

0.7

073

4

18

971

73

05

51

.7

39

.9

13

1.7

8

63

81

6

97

8

8.2

1

1.9

2

1.0

1

.7

29

21

0.7

072

2

30

947

11

058

42

.0

60

.2

10

8.6

9

99

37

9

45

3

1.8

2

1.8

1

4.8

3

.2

Note

the

erro

r on t

he

assi

gned

age

is e

stim

ate

to b

e 0.7

5 M

a.

52

Tab

le 3

: E

lem

enta

l co

mposi

tion (

mg/L

) an

d8

7S

r/86S

r ra

tio o

f G

a’as

h 2

bore

hole

Dep

th m

8

7S

r/8

6S

r

SiO

2

Ca

M

g

Mn

F

e A

l S

r N

a

K

SO

4

f C

aC

O3

Ass

. A

ge

±0

.75 M

a

44

13

0.7

074

2

74

29

410

1

48

60

10

81

72

36

76

<1

4

04

2

0.1

0

44

16

0.7

074

5

54

19

470

1

02

90

4

24

<1

1

8

24

<1

2

12

4

0.0

7

44

19

0.7

073

8

8

21

180

1

03

80

4

21

<1

2

5

22

<1

2

56

2

0.1

1

44

22

0.7

073

8

80

29

320

1

50

50

10

36

<1

3

9

78

<1

3

86

2

0.0

9

44

25

0.7

074

6

98

27

550

1

39

20

6

47

<1

2

8

41

<1

3

67

9

0.1

0

89

19

950

1

01

20

4

43

<1

1

9

13

<1

2

56

8

0.1

0

44

31

0.7

075

1

29

1

30

150

1

51

30

9

14

5

<1

3

7

56

<1

4

75

8

0.1

0

19

2.8

44

34

0.7

075

6

22

3

21

910

1

11

30

7

78

<1

2

6

42

<1

3

15

5

0.1

0

19

4.9

44

37

0.7

074

8

33

8

27

940

1

38

50

8

11

7

<1

4

5

57

<1

3

01

4

0.1

1

19

4.1

44

43

0.7

075

5

25

5

31

250

1

59

80

8

15

1

<1

3

6

11

4

<1

4

49

4

0.0

9

19

4.2

44

46

0.7

075

2

19

3

27

730

1

39

80

8

17

8

<1

4

0

56

<1

4

71

6

0.1

0

19

5.0

44

49

0.7

075

1

18

9

28

670

1

46

70

7

98

<1

3

0

12

<1

3

99

4

0.0

9

19

4.5

44

52

0.7

075

1

27

6

26

770

1

31

10

8

10

4

<1

3

0

59

<1

3

79

9

0.1

1

19

4.2

44

55

0.7

075

2

49

8

36

960

1

97

10

8

13

6

<1

4

3

42

<1

4

17

1

0.0

7

19

4.5

44

58

2

54

40

200

1

99

20

8

59

<1

4

5

53

<1

4

60

8

0.1

1

44

70

0.7

075

5

65

22

260

1

07

90

5

17

<1

1

9

-23

<

1

27

60

0.1

2

19

4.6

44

73

0.7

075

4

15

9

35

840

1

70

20

6

55

<1

2

8

9

<1

4

23

7

0.1

3

19

5.4

44

76

0.7

075

0

76

21

800

1

09

10

4

25

<1

2

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56

תקציר

יורא בתת הקרקע של מערב צפון -המטרה העיקרית של מחקר זה הייתה לאפיין את המעבר טריאס

ובמידת האפשר לשייך גילים ישראל בעזרת ביוסטרטיגרפיה, סביבות השקעה, תהליכים דיאגנטיים

–מעבר טריאסשניים מהם ב. שלושה קידוחים נבחרו למחקר; Srנומריים בעזרת כרונוסטרטיגרפיה של

(, וקידוח אחד ללא 1ואשר עתלית 3 הו)אלי בסביבת המעבר פעילות וולקניתל יורא מכיל עדויות ישירות

שה הניסיון האזורי הראשון להגדיר את בעבודה זו נע(. 2געש ) במעבר שום עדות לפעילות וולקנית

, מעוגנים ע"י 87Sr/86Srכרונוסטרטיגרפיה של יחסי יורא בתת הקרקע של צפון ישראל ע"י-מעבר טריאס

שקפי סלע של מטחני קידוח 240ביוסטרטיגרפיה כאשר ניתן. מיקרופאליאונטולוגיה ומיקרופציאסים של

דוגמאות מטחן 140. בנוסף, CLוסקופים של אור חודר ו מהאינטרוולים הרלוונטיים נבחנו תחת מיקר

יחד עם הגדרת אלמנטים 87Sr/86Sr ימאותם אינטרוולים עברו אנליזה להגדרת יחס שלמות שהוצאו

Srאחת המסקנות העיקריות של עבודה זו היא כי ניתן בהחלט ליישם סטרטיגרפיית עיקריים וקורט בהם.

על חומר מקידוחים עם הזהירות הראויה כאשר מחשבים את הגיל לפיה.

מ', מעל הפאזה הוולקנית העיקרית, והיחידות 2855יורא מוקם בעומק -, מעבר טריאס3 הובקידוח אלי

הקרבונטיות המתחלפות עם וולקנים ומעל בסיס תצורת נירים )בתוך החלק הדולומיטי התחתון(; בכך

ליורא תחתון. ליחסהלקנית בעיקרה כטריאסית ללא פעילות וולקנית מאוחרת שניתן הוגדרה הפאזה הוו

-מ', אך המעבר טריאס 4532מ.ש.( בעומק 197, התוצאות העלו גילים של יורא תחתון )2בקידוח געש

.עדין יורא לא אובחן

סביבה ריפית עם הוולקנים אינטרוול קרבונטי המכיל עדויות ל בסיס, נמצאה מעל 1בקידוח אשר עתלית

פורמיניפרים טריאסיים, המחזק את הקשר בין האירועים הוולקנים להופעה של המערכת הריפית. על

שוב.בסיס הביוסטרטיגרפיה, גבול טריאס יורא צריך להיות גבוה בהרבה ממה שהיה מקובל לח

ום הדוגמאות במשך נכשלה בחיזוי גילים של קרבונטים בסביבה וולקנית, יתכן עקב זיה Srסטרטיגרפיית

השנים אך בהחלט יתכן שנוכחות הוולקנים שינתה יחס האיזוטופים במי החללים בעת השקעת הצמנטים

בהם.

מראה מעבר טיפוסי של 2וגעש 3המעבר של הטריאס העליון אל תוך היורא התחתון בקידוחי אליהו

לופין עם סביבות אואואידיות סביבת השקעה פרוקסימלית קרבונטית רדודה שהכילה מרבדי אצות לחי

לפני, במשך ואחרי המעבר בין התקופות. תצפיות אלו דומות להופעה הנרחבת של גיר סטרומטוליטים

הרדודים. התטיס אזורישל פנים המדף הקרבונטי שאפיין את הטריאס העליון של האלפים ושאר

יורא, ללא פער -יאסהפלטפורמה הקרבונטית הרדודה שהתקיימה בקנה מידה נרחב במעבר טר

סטרטיגרפי ניכר )נכון לעבודה זו( מאשר בעיקר שאזורית המעבר טריאס יורא התרחש דווקא תחת

מתקופת מתיחה אקטיבית לפאזת שקיעה פסיבית של שולי שקט טקטוני ווולקני, והא כנראה מציין מעבר

(.saggingיבשת )

משרד התשתיות הלאומיות האנרגיה והמים

המכון הגיאולוגי

בסביבה בתת הקרקע של צפון ישראל, יורא -מאפייני מעבר טריאס

קרבונטית תחת השפעה וולקנית: סביבות השקעה, היסטוריה דיאגנטית

Srוהכרונוסטרטיגרפיה של

דורית קורנגרין ויהודית הר לבן

Report GSI/08/2016 2016 ינואר, ירושלים