THE MINISTRY OF NATIONAL

INFRASTR UCTURES

GEOLOGICAL SURVEY OF ISRAEL

NOTES ON THE GEOLOGY OF

) Based on the 1:50,000 geological maps of Har .. ..,.. '~""~~.ג~~:!,!

D. Mor, H. Michelson, Y.

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State of IsraeI

The Ministry ofNationaI Infrastructures

GeologicaI Survey of IsraeI

NOTES ON THE GEOLOGY OF THE GOLAN HEIGHTS

(Based on the 1:50,000 geological maps ofHar Odem and Qazrin sheets by D. Mor

and Gamla sheet by H. Michelson and D. Mor)

by

D. Mor1•2, H. MicheIson3, Y. Druckman1, Y. Mimran1, A. Heimann1, M. Goldberg1

and A. Sneh1

1 Geological Survey ofIsrael, 30 Malkhei Israel St. Jerusalem 95501 2 Qibbuz Merhavya 3 Water Planning for Israel, Tel Aviv

Descriptions o[

Volcanic units in the Golan heights by

DoronMor

Sedimentary units in the northem Golan by

Amihai Sneh, Yehezkeel Druckman, Ya' akov Mimran, Ariel Heimann, Moshe Goldberg and Doron Mor

Sedimentary units in the southern Golan by

Haim Michelson

Report GSI/15/97

Jerusalem, September 1997

2 r r CONTENT

4 .................................................................................................................. Preface 5 ........................................................................................................... ntroduction ז

6 ........................................................................................................... Stratigraphy 6 ....................................................................................................... 1. Arad Group 6 ......................................................................................... 1.1. Hennon F onnation 7 ............................................................................................ 1.2. Kidod Fonnation 7 ................................................................. 1.3. Be'er Sheva and Haluza fonnations 8 .................................................. 2. Kumub Group and lower parts of Judea Group 8 ............................................................................................... 2.1. Bhannes Basalt 8 ............................................................................................ 2.2. Hatira Fonnation 8 .................................................................................... 2.3. Ein el Asad Fonnation 9 ............................................................................................ 2.4. Kati'h Fonnation 9 ......................................................................................... 2.5. Mas'ada Fonnation 9 ................................................................. 3. Judea Group, middle and upper parts 9 ............................................................................................ 3.1. Yagur Fonnation 9 .................................................................................... 3.2. Deir Hanna Fonnation

10 ......................................................................................... 3.3. Sakhnin Fonnation 10 .............................................................................................. 3.4. Bina Fonnation 10 ....................................................................................... 4. Mount Scopus Group 10 ......................................................................................... 4.1. Menuha Fonnation 10 ........................................................................................ 4.2. Mishash Fonnation 10 .......................................................................................... 4.3. Ghareb Fonnation 11 ........................................................................................... 4.4. Taqiye Fonnation 11 ................................................................................................... 5. Avedat Group 11 ......................................................................................... 5. 1. Adulam F onnation 11 ........................................................................................ 5.2. Maresha Fonnation 12 .................................................................................. 5.3. Bar Kokhba Fonnation 12 .................................................................................................... 6. Saqiye Group 12 ................................................................................................ 6.1. Fiq Fonnation 12 ............................................................................................ 6.2. Susita Fonnation 13 ................................................................................................ 6.3. En Gev Sands 13 ......................................................................................... 6.4. Hordos Fonnation 14 ............................................................................................... 7. Dead Sea Group 14 ............................................................................ 7.1. Bira and Gesher fonnations 15 ........................................................................................... 7.2. Gadot Fonnation 15 ........................................................................................... 7.3. Hazor Fonnation 15 ............................................................................................... 7.3.1. Si'on Gravel 15 ......................................................... ; ................................... 7.3.2. Buteiha Gravel 16 .................................................................................. 7.4. Kefar Yuval Travertine 16 ............................................................................................... 7.5. Dan Travertine 17 ................................................................................................... 8. Bashan Group 17 .................................................................................................. 8.1. Cover Basalt 18 .................................................................................................... 8.2. Eitar Basalt 18 ............................................................................................. 8.3. Ortal Fonnation 19 ............................................................................................... 8.3.1. Dalwe Basalt

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8.3.2. Sheivan Scoria ............................................................................................ 19 8.3.3. Hasbani Basalt ............................................................................................ 20 8.3.4. Yarmouk Basalt .......................................................................................... 20 8.4. Golan Basalt .................................................................................................. 21 8.4.1. Muweisse Basalt ......................................................................................... 21 8.4.2. Keramim Basalt .......................................................................................... 22 8.4.3. Odem Scoria ............................................................................................... 22 8.4.4. 'En Ziwan Basalt ........................................................................................ 23 8.4.5. Avital Tuff .................................................................................................. 23 8.4.6. Raqqad Basalt ............................................................................................. 24 8.4.7. Berekhat Rarn Tuff ..................................................................................... 24 8.4.8. Sa'ar Basalt ................................................................................................ 25 9. Undivided basalt ............................................................................................... 25 10. Alluvium ......................................................................................................... 25 Geological structure ............................................................................................. 25 1. The Hennon anticline ........................................................................................ 26 2. The geological structure beneath the volcanic plateau ....................................... 26 3. Faulting ............................................................................................................ 27 4. The volcanic alignments .................................................................................... 28 Geological history ................................................................................................. 29 Economic Geology ............................................................................................... 31 Acknowledgments ................................................................................................ 32 References ............................................................................................................ 32

4

PREFACE r notes are provided for three 1 :50,000 geological maps: Har Odem, Qazrin yזExplanato

and Gam1a, covering the area of the Golan heights. The stratigraphic column of the rocks

g area extends ftom the Jurassic to the Quatemary. It comprises מithe mapp מig out מicropp

the Hermon מiunits attributed to 8 groups. The Arad and Kumub groups, exposed

the northem Golan, and the Avedat מistructure; the Judea and Mount Scopus, found only

, the south. Al1 these units מiand lower parts of the Saqiye which build the canyon cliffs

thickness, are marine. The upper parts of the מiage, 3000 m מiJurassic to oligocene

ental and are. about מiMiocene, Saqiye Group, with the exception of few thin beds, are cont

300 m thick. The overlying Plio-Pleistocene Bashan Group build the volcanic plateau ofthe

Golan height, is of varying thickness, up to few hundreds of meters, and comprises basalts

as welI as pyroclasts. Contemporaneously, sediments of the Dead Sea Group accumulated

within the subsided Rift to the west of the Plateau

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Still to be completed before publication ofthe final edition ofthe maps are: a) the detai1ed

) the Hermon area; b מistratigraphy ofthe thick Jurassic section ofthe Hermon Formation

the Hermon structure and the Lower Cretaceous מiresearch on the tectonic elements

the map was provided by A. Shimron (1986; and מicluded מivolcanism; data on the latter

written comm., 1987) and is only preliminary; c) the stratigraphic division of the "undivided

the southwestem part מig of the tectonic features מithe westem Golan; d) mapp מi" basalts

. of the Qazrin sheet on the westem side of the Jordan River; and e) dating additional sites

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The following explanatory notes relates to the geology mapped and displayed in three

1:50,000 sheets: Har Odem (Mor, 1987a), Qazrin (Mor, 1987b) and Gamla (Michelson and

Mor, 1985). The boundaries of these sheets, being different :&om those of the regular

topographic sheets of the Survey of IsraeL were chosen to cover the whole of the Golan

. heights which is one phisiographic unit, in 3 sheets

This physiographic unit is divided into two and is highly in keeping with the geological

: cture stזu

1. the folded Mount Hermon north ofNahal Sa'ar, built predominately ofthick Jurassic

limestones and some shales and

2. the young Golan volcanic plateau south ofNahal Sa'ar, that slopes :&om NNE to SSW

and on which tens of volcanic cones stand out. Likewise, the location of the cliffs, and

hence of the canyons, in the westem Golan heights, towards the Hula Valley and the

. Kinneret, is dictated by the main faults ofthe Rift Valley

The entire area drains directly or indirectly to the Jordan basin. The water divide, which

runs :&om north to south in the eastem part of the Golan heights, divides the area into twO

secondary basins: the larger westem one drains directly into the Jordan River and Lake

Kinneret, the smaller eastem one, to the Raqqad and Yarmouk rivers and through them, to

, the Jordan. Water t10ws in the Golan streams during most ofthe winter and spring months

and in some, also during the summer. On the Golan plateau itself the streams are quite

shallow, but they deepen, cutting canyons as they approach the Hula Valley, Lake Kinneret

and the Yarmouk and Raqqad rivers. The climate is Mediterranean, with average annual

precipitation ranging :&om around 1100 mm at the swnmit of Mount Hermon down to

. around 500 mm in the southem Golan heights

The geological mapping ofthe volcanic units in the Golan heights on a 1 :50,000 scale was

carried out in several stages in the course of the years 1967-1986, as part of research

projects on the volcanism ofthe Golan heights (Mor, 1973, 1985, 1986). The sedimentary

units ofthe northem Golan are presented following Sneh et al. (1985), who based their map

mainly on previous mapping ofthe area (see below). Some.ofthe dip measurements were

provided by P. May (written comm., 1986). The sedimentary units of the southem Golan

.) 1979 , 1972 ( were studied and mapped by Michelson

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The Mount Hermon area was previously mapped by Dubertret (1954, 1960) within the

framework of mapping the Levant. The Golan was previously mapped by Ponikarov et al.,

(1963-64) as part ofthe geological map of Syria. Golani (1962) carried out initial mapping

in the En Gev area. After 1967 the northem part of the Golan and the Hermon were

mapped by Saltzman (1968) and by Michelson (1975). Part of the central Golan was

mapped by Netser (1982). Heimann (1985) mapped the northem Hula Valley.

STRATIGRAPHY

The stratigraphic column of the rocks cropping out in the mapping area extends from the

Jurassic to the Quatemary (Fig. 1). Fol10wing is a brief decription ofthe mapping units. The

division of the sedimentary rocks was made on the basis of lithostratigraphic criteria; that of

the volcanic formations and members was made using morphological as welI as

chronostratigraphic criteria.

Fossil identification was made at the Geological Survey and at the Israel Petroleum

Institute; the radiogenic age determinations were carried out in the Survey's geochronology

laboratory.

1. ARAD GROUP (Jurassic)

The lithostratigraphic fonnations of the Arad Group in the mapping area are: Hermon,

(Dubertret, 1975) Kidod, Beer Sheva and Haluza (Goldberg, 1969, 1980; Goldberg et al.,

1981), which are units J4, J5, J6 and J7 ofDubertret (1960, 1963), respectively. These rock

units extend chronostratigraphically from the Middle Jurassic Bathonian stage into the

Upper Jurassic, Upper Oxfordian stage.

Derin (1969) found a high degree of similarity between the Hermon and the Negev

sequences.

1.1 Hermon Fonnation (Jmh)

Except for a few shales and calcareous shale beds in its upper parts, the Hermon

Formation is built mainly oflimestone (biomicrite in most cases) and some dolomite. A few

calcarenite beds, occasionally oolitic, are scattered throughout the sequence. The formation

is 623 m thick, but its base is not exposed in the mapping area. It covers almost all of

Mount Hermon and was divided into three members (from bottom to top): Mizpe-Shlagim,

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massively bedded and cliff forming - 170 m thick; Bol'an, finely bedded - 95 m thick; and

cluding מiMa'ale Golani, whose rocks are highly fi"actured - 358 m thick. Karstic features

the latter. The upper part of the formation was correlated with the מidolines are common

. upper part ofthe Zohar Formation in the Negev

) 1.2 Kidod Fonnation (Juk

, The Kidod Formation is 155 m thick; it consists of shales, for the most part calcareous

the upper part of מipyritic and lignitic. These are generally light gray-brown to yel10w, but

the middle part the shales מI. the formation they are dark gray (''black'') and gray-brown

tra biosparite, occasionally מialtemate with thinly bedded limestones, mostly calcarenite and

oncolitic; in the lower part of the formation the shales are fossiliferous; ammonites and

belemnites (mostly pyritic and/or hematitic) are very abundant. There are also some plant

the Majdal מia few localities מiremains and vertebrate bones. Basaltic intrusions are found

. Shams-Qal' at Nimrud area

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) 1.3 Be'er Sheva and Haluza fonnations (Jub and Juh

The Be'er sheva Formation is 100 m thick and consists mainly of light gray and whitish

sponge spicules, and intrabiosparite). The limestones מiplaces rich מi, limestones (biomicrite

are well bedded; in the lower part of the formation the beds are thin and alternate with dark

gray shales; in the upper part they are massive and cliff-forming. The upper part ofthe Be'er

Sheva Formation is characterized by the presence of oncolites, stromatoporoids and

, echinoid fi"agments. The Upper Jurassic Balanocidaris glandifera, with pear-shaped spines

, called the "Jewish Stone", has been well known since Crusader times for its magical

. powerful healing properties

The Haluza Formation is 125 m thick and consists mainly of limestones. Yellow-brown

intrabiosparites, occasionally cross-bedded and oolitic, and some micrites commonly

alternate with moderately to finely bedded, fossiliferous calcareous shales with

underlain by basalt flows related to the מistromatoporoids and onclolites. The fonnation

Lower Cretaceous volcanic phase. No distinction was made on the map between the Be'er

. Sheva and Haluza formations in the Hermon area; they were treated there as a single unit

Both fonnations were first described in the northem Negev (Coates et al., 1963), where

. their age was determined as Upper Jurassic

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2. KURNUB GROUP and LOWER PARTS of JUDEA GROUP (Lower Cretaceous)

Five lithostratigraphic units crop out on the eastem slopes of Mount Hennon. These units

are widely distributed in Lebanon.

.) b) (mispelled 'Banas' on map 32.1ז Bhannes Basalt (Kl

This unit ranges in thickness between 0 and 30 m; it unconformably overlies the Beer

Sheva and Haluza fonnations and is underlain by the Hatira sandstones. According to

Shimron (1988, 1989a,b), Shimron and Lang (1989) and Shimron and Peltz (1993) this unit

, comprises a sequence of layered basalt flows, dykes, diatrem breccia pipes, pyrocastic

epiclastic and lacustrine rocks and is part of the Nimrod magmatic cycle of Shimron

.) 1989b (

, Saltzman (1968) correlated the basalts with the Bhannes basalts in Lebanon (Dubertret

1963) and was of the opinion that, Iike those is Lebanon, the basalts in the Hennon are of

Upper Oxfordian age. However, radiogenic dating of the basalts ffom the many intrusions

within the Hennon Fonnation as well as those overlying the Haluza Fonnation in the

118 , Hennon (Mor et al., 1984; Shimron and Lang, 1988) yielded a Lower Cretaceous age

to 113 m.y. A wider range, 133 to 88 m.y. was reported by Shimron and Lang, (1989). The

use ofthe name Bhannes for the basalts in the Hermon might therefore be highly misleading

; even though the Bhannes basalts in Lebanon have not been radiometrically dated as yet

. another name should be used in future editions

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2.2 Hatira Formation (Klh)

The Hatira Fonnation, tenned Gres de Base by Dubertret (1960), is built ofsandstone and

is up to 85 m thick (Saltzman, 1968; Sneh, 1974). 1t unconfonnably overlies the Nimrod

Volcanics, and, contrary to other places in Lebanon or in the Galilee where it is covered by

marls, in the slopes of the Hennon it is overlain by limetones. i ) 2.3 Ein el Asad Formation (Klei

.) 1968 , The Ein el Asad Formation is built oflimestone and is about 65 m thick (Saltzman

a number of places, e.g., close to Ein Qunya, it cou1d not be identified because of מI

Iandslides. The formation name was given by Eliezri (1965) and is synonymous with Falaise

.) 1960 ( de Blanche, unit C2b, defined by Dubertret

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) 2.4 Kati'h Formation (Klka

The Kati'h F onnation, which is exposed on the slopes of Mount Hennon, was first

described by Saltzman (1968). It is about 65 m thick and confonnably overlies the

, limestones ofthe Ein el Asad Fonnation. The Kati'h Fonnation is built of sandstone, marl

and some limestone. In the Galilee the coaelative fonnation, the "Orbitolina horizons" unit

described by Rosenberg (1960) and the Hidra Fonnation described by Eliezri (1965) lacks

sandstones. Mimran (1969) described the sandstones at the base ofthe Tammun Fonnation

. Samaria as coaelative to the Kati'h Formation מi

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) 2.5 Mas' ada Formation (Klma

The name Mas'ada Formation was given by Saltzman (1968) to the 140-250 m limestone

unit overlying the Kat'ih Formation. Dubertret (1960) considered this unit as the base ofthe

Cenomanian-Turonian section (C4). The ''Knemiceras'' marl beds (Albian), which overlie

Lebanon and to that in Upper Galilee, are מithe section equivalent to the Kati'h Fonnation

missing in the Hennon area; hence the exact stratigraphic position of the Mas' ada

. Fonnation is not clear

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r ) DLE AND UPPER PARTS (Albian-Turonian 3ש. JUDEA GROUP, M

The mapping, fol1owing Saltzman (1968), is based on the division ofthe group into four

units: Cel-3 (Albian?-Cenomanian) and t (Turonian). The accepted stratigraphic

. northem Israel has been adopted, accordingly מinemenclature

) 3.1 Yagur Formation (Kuya

The Yagur Formation (Ein Sa'ar Formation of Saltzman, 1968) is built of dolomite and is

.) 1975,1979 the Ya'afuri Val1ey according to Michelson, מiabout 150 m thick (40 m thick

. places wel1 bedded מiThe dolomites are gray, porous, massive, and

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3.2 Deir Hanna Formation (Kude)

The Deir Hanna F ormation consists of limestones, dolomites, chalks and marls and is

about 400 m thick (on1y 210 m according to Michelson, 1975, 1979). Facies changes within

the fonnation are common.

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3.3. Sakhnin Formation (Kusa)

The Sakhnin Formation is built of a series of dolomites which, according to Saltzman

(1968), are 100 to 170 m in thickness (In the eastem Hermon near Mazra'at Bet Jin a

section of 206 m was measured by Michelson, 1975). The dolomites are gray, generally

porous, well bedded, and form cliffs.

) 3.4. Bina Formation (Kub

The Bina Formation is built of limestone and dolostone and is ftom about 30 to 70 m

and, as in other places in northem Israel, it is difficult to separate ftom the Sakhnin ~ thick

Formation because of intensive dolomitization. The limestones and dolostones are well

. thickness מibedded, with beds ranging between 20 and 100 cm

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4. MOUNT SCOPUS GROUP (Senonian-Lower Eocene)

The four formations ofthe group were studied by Mimran et al. (1985).

4.1. Menuha Formation (Kum)

The Menuha F ormation is built of white, massive, ftactured chalk and is about 40 m thick.

Its age is Santonian.

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4.2. Mishash Formation (Kumi)

The Mishash Formation is built ofbrecciated chert ofCampanian age. It crops out in one

place only, at Tel Manfuha, and is about 4 m thick (Chert blocks are abundant on the slope

below). r ) 4.3. Ghareb Fonnation (Kug

The Ghareb Formation is built ofup to 12 m ofMaastrichtian chalk. In Nahal Orevim, the

however, at the base of the formation ~ g מiunderlying Mishash Formation cherts are miss

the מithere is a conglomerate just 30 cm thick, containing chert pebbles which originated

Mishash Formation, as well as limestone and dolomite pebbles. Three kilometers to the

north, east ofKibbutz Shamir, beds ofthe Ghareb Formation unconformably overlie beds of

. the Deir Hanna Formation f8I

11 r 4.4. Taqiye Formation (Tlt)

The Taqiye Fonnation is built of marl and is about 30 m thick, but contrary to other

places in Israel where it is of Paleocene age, in the Golan the Taqiye is of Eocene age. At

Tel Manfuha the Maastrichtian chalks ofthe Ghareb Fonnation are completely missing and

the marls cover the chert beds ofthe Mishash Fonnation.

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) 5. A VEDAT GROUP (Lower-Middle Eocene

Outcrops of the A vedat Group in the southem Golan heights point to a basinal

sedimentary province, whereas those in the north point to a continental shelf environrnent

uth, the Adulam and Maresha formations are exposed; these were סsSneh, 1988). In the (

studied in detai1 by Michelson (1972; 1979) and the explanatory notes are based on his

. descriptions. In the north the Adulam, Timrat and Bar Kokhba fonnations crop out

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5.1. Adulam Formation (Ea)

The lower part of the Adulam F onnation is not exposed in the southem Golan heights,

but data ftom the Nahal Mezar boreholes indicate that it overlies the Taqiye Fonnation. The

fonnation is confonnably overlain by the Maresha Fonnation. The Adulam Fonnation is

built of layers of hard yellowish-white chalk with chert lenses throughout the section.

Limestone horizons also occur and intermittent marly units emphasize the bedding. The

fonnation is about 250 m thick, of which about 200 m are exposed; the exposures are

mainly in the Yarmouk area. The age of the fonnation is Lower to Middle Eocene

(Michelson and Lipson, 1986).

In the northem Golan heights in the Tel Warda borehole, an approximately 50 m section

of chalk and limestone with chert lenses was penetrated. This section was attributed to the

Adu1am Fonnation. In the GaIilee this facies characterizes the Timrat Formation. A 17 m

chalky unit in the Shamir ''Kipuka'' was mapped belonging to the Adu1am Fonnation.

However, the upper part, in which there are hard limestones, may actual1y belong to the

Timrat Fonnation.

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) 5.2. Maresha Formation (Emr

The Maresha Fonnation confonnably overlies the Adu1am Foramtion. Its upper part is

. vered by the Fiq Fonnation, the Hordos Formation or the Cover Basalt סctruncated and

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The formation bui1ds moderate slopes, is densely jointed and usually not bedded. The

rocks comprising the formation are chalks, and grayish or yellowish-white marls. In places

there are chert or limestone horizons. The formation in Nahal Mezar is about 180 m thick' ,

in Wadi Samakh only about 120 m are exposed. The age ofthe fonnation is Middle Eocene

(Michelson and Lipson, 1986).

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) 5.3. Bar Kokhba Formation (Ebk

iThe Bar Kokhba Fonnation is bui1t of limestone of Middle Eocene age. Its exposuresמ

in the subsurface (T eI Warda borehole) it is ~ the Har Odem quadrang1e are about 20 m thick

. at Ieast 40 m thick r

6. SAQIYE GROUP (Upper Eocene-Miocene)

Rocks of the Saqiye Group crop out only in the Gamla quadrang1e. f'1I'II

01) ( 6.1. Fiq Formation

iThe Fiq Fonnation was first described by Michelson (1972). Its type section is foundמ

Nahal En Gev (Wadi Fiq) north of Susita at coordinate 2124/2435, where it attains its

. maximum thickness, 45 m

The formation unconfonnably overlies the Maresha Fonnation. A hard ledge at its base

. fonns a step that is prominent in the Iandscape

marine מiThe rocks comprising the fonnation are glauconitic and detrital limestones rich

imicrofauna and also chalks and marIs. There are chert Iensesמ iplacesמ I. the upper partמ

the base, traces of marine burrowers and large concentrations of barite are found. The

pockets and comprises up to 30% of the rock, though it מiglauconite is scattered or occurs

-gradually decreases upwards. The glauconitic rock is clearly recognizable by its greenish

. brown color. The fonnation is ofUpper Eocene to Oligocene age

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) 6.2. Susita Formation (Os

it confonnably overlies the Fiq ~ The Susita Fonnation was studied by MicheIson (1972)

. Formation and is overlain unconfonnably by the En Gev Sands or the Hordos Formation

g the Susita Formation are: limestone, marl, greenish (g1auconite) sandy מiThe rocks build

, dolomite with fossiIs, chert, quartzite and loose yellow sand. The limestones are sandy

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bioclastic, chaIky, marly'and highIy fossiIiferous~ lumacheIIes are common. A pecten horizon

characterizes the base of the formation.

The formation attains its maximum thickness, 145 m, in the Susita area, thinning to 25 m

in the cliffs ofHa'On. It is divided into two members: 1) Ha'On - 100 m thick, consisting of

marIs and caIcareous marls, containing marine fossi1s; 2) Nuqeib - around 45 m thick,

consisting of limestone, chaIk, sand, and reddish chert horizons, and devoid of fauna. The

age of the formation is Oligocene to lowermost Middle Miocene.

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) v Sands (Me Gi6.3 י En

The En Gev Sands (GoIani, 1962, emended by Michelson, 1972) overIies the Susita

Formation with an anguIar unconformity between. These sands represent the beginning of a

continental cycle. They are yellow, loose or slightly cemented by carbonate; there are a few

laminar lacustrine limestone horizons in the upper part of the formation (see aIso Giveon,

, 1984). The sands consist mainly of quartz grains and some redeposited glauconite grains

transported by wind and apparently deposited in a 10caI fi-eshwater lake. The formation is

around 90 m thick and crops out in the Susita-Qeren En Gev and Ha'On cliffs area. It is of

. Middle-Upper Miocene age

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r 6.4 Hordos Fonnation (Mh); Lower Basalt (MJiI)

The Hordos Formation overlies the Susita Formation, or the En Gev Sands where

present, with an angular unconformity between. Overlying the Hordos Formation is the

Gesher Formation; where the latter is absent, it is overlain by the Cover Basalt.

The sediments were deposited in fteshwater lakes and in a fluvial system of a broad

continental basin. The facies changes are marked and numerous. The dominant rocks of the

Hordos Formation are: congIomerates, caIcareous sandstones, marls, limestones, sandy

limestones, si1tstones and mudstones. Along the cliffs of Ha'On three members are

differentiated by their coIors: the Iower Red Member; the middle White Member; and the

Upper Member, which lacks a characteristic color.

The formation is 242 m thick in the Ha'On cIiffs, and 208 m in Wadi Samakh, whereas

towards the south, north and east it gradually thins downto severaI tens of meters.

At the base of the formation a number of basaIt flows interfinger. These fIows range in

thickness between 5 and 30 m. According to Mor (1986), the radiogenic age ofthe basaIt is

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14

about 13 m.y.; according to Sha1iv and Steinitz (1988) and Sha1iv (1991), it is about 15 m.y.

These ages are close to those ofthe Lower Basa1t described from the centra1 Jordan Valley

by Schulman (1962). Hence the age of the whole of the Hordos Formation is Middle

Miocene.

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7. DEAD SEA GROUP (Plio-Pleistocene) r!!I!I [

t7.1. Bira and Gesher formations (Pg); Intermediate Basalt (M(3i); Fejjas TufT (P(3ן

;) 1962 In the centra1 Jordan Valley two distinct formations were distinguished (Schu1man,

in the lower, the Bira Formation, marine fauna is found, whereas the upper, the Gesher

Formation, is continenta1. In the Golan heights the entire section is around 80m thick and

. most of it points to a continenta1 environment

Michelson (1972) distinguished three tiny outcrops of ostreid lumachelle, resembling that

of the Bira Formation in the central Jordan Valley. However, this was not sufficient to

justify dividing the section into two separate formations. The section is bui1t of lithographic

limestone, ca1careous sandstone, mudstone and conglomerate (the 'lithographic limestone

facies' in the Tawafiq area) and of oolitic limestone and marl rich in fauna (the 'ooIitic

.) limestone facies' in the Aaqeb area

Near Kh. Nuqeib (coord. 2111/2439) a basalt tlow separates between the ostreid

Iumachelle above and the Hordos Formation below. Radiogenic dating of his basa1t yielded

an age of 6.42 m.y., and thus being correlative with the Intermediate Basa1t that interfingers

with the Umm Sabune conglomerates and the Bira marls in the centra1 Jordan Valley

Schulman, 1962). Intermediate basa1ts were a1so reported by Sneh, Lang and Ha1icz (in (

. prep.) from outcrops in Naha1 Dalliyot

Near Tel Qazir (coord. 2085/2350), a friable weathered basa1t tlow in the section yielded

an age of 5.19:1:1.16 m.y. and should thus be ascribed to the Fejjas Tuff unit (that

.) 1962 , interfingers with the Gesher Formation in the centra1 Jordan Va11ey; Schulman

Likewise, weathered basa1t tlows are also found in the section in Naha1 Kanaf (coord. of

base 21345/25193), each about 6-8 m thick with a latera1 distribution of severa1 hundred

4.5::1:0.2 meters. Mor (1986) checked the radiogenic age ofthe lower f10w and found it to be

m.y., i.e., Pliocene; Sha1iv and Steinitz (1988) and Sha1iv (1991), however, dated two

~

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samples trom the upper t10w and found them to be 5.2:1:0.15 m.y. (coord. 21350/25215) and

5.4:I:0.5 (coord. 2150/2510).

The following four formations are ascribed by Horowitz, 1979, to the Hula Group.

7.2. Gadot FormatioD (Qg)

The formation, which crops out near Kibbutz Gadot, is built of 25 m of white lacustrine

chalk. (Picard, 1952~ Horowitz, 1979), which interfingers westward with the Hazor gravel.

According to Heimann et al. (1990), the chalks are younger than the Dalton basalts and

older than the Yarda basalts, and thus approximately 1.5 m.y. old.

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7.3 Hazor Formation (Qz)

The Hazor Formation was described trom the Hula Valley (picard, 1952). Within the

mapping area the formation was devided into two members (Mor, 1986).

7.3.1. Si'on Gravel Member (Qzs)

The Si' on Gravel Member builds the fans of the rivers t10wing out of Mount Hermon into

the Hula Valley. The type section, which is about 80 m thick, is found at Giv'at Hamra

(coord. 2138/2950), close to where Nahal Si'on flows into the Hula Valley. It is overlain by

the Dan Travertine~ its base is not exposed. The unit consists mainly of well-rounded,

unsorted, limestone pebbles of the Hermon Formation, and of some travertine, occurring

either as cementing materia1 or as separate horizons.

Inasmuch as the pebbles of the unit have been accumulating trom the very beginning of

the formation ofthe present Jordan Rift Va1ley, at least trom the post-Cover Basalt stage,

the age of the unit is evidently Upper Pliocene-Recent.

!81

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7.3.2. Buteiha Gravel Member (Qzb)

The Buteiha Gravel Member builds the fans of the rivers draining the Golan heights to the

Hula Valley and the Bet Zayda (Buteiha) Va1ley. In two exploratory boreholes, one near

Bet Habeq and the other near Sheikh Hader in the Buteiha Va1ley (Michelson, 1979), 102 m

ofthe unit was penetrated without reaching its base. f1IIiI

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The unit consists almost entirely of rounded to sub-rounded, uncemented and unsorted

basalt pebbles. Limestone pebbles are found in the fans of those rivers which drain limestone

terrain (e.g., Nahal Hemdal).

The Buteiha Gravel is equivalent in age and genesis to the Si'on Gravel unit.

7.4 Kefar Yuval Travertine (Qky)

The Kefar Yuval Travertine was studied in the Hula Val1ey (picard, 1963~ Heim~

1985). The type section is found at the entrance to HaGosherim (coord. 20845/29215) and

is 25 m thick.

The formation is built of two monomineral-calcitic travertine facies: a) a massive white­

brown, soft, homogenous travertine devoid of fossils~ and b) a travertine containing fossils

of various plants, mostly stems and leaves.

The formation overlies the lower flows of the Hasbani Basalt~ it is overlain by either

younger Hasbani Basalt flows, the Dan Travertine or, most usually, by recent soils.

The age ofthe formation is Upper Pleistocene. Horowitz (1979) estimated its age as 0.15

m.y. on the basis of its pollen, whereas Schwarcz et al. (1980), using the Th/U method,

estimated it to be older than 0.35 m.y .. On the basis of field relationships between the

travertine and a dated basalt flow, Heimann and Sass (1989) estimated the age of the base

to be older than 0.8 m.y.

7.5 Dan Travertine (Qd)

The Dan Travertine was studied in the northem Hula Val1ey (Picard, 1963~ Snir

Travertine of Heimann, 1985). The type section is found in the gorge of Nahal Hermon,

near the Banyas waterfal1 (coord. 2140/2941) and is about 15 m thick.

The formation, which is the uppermost sedimentary rock unit mapped, overlies the Dalwe

Basalt, the Si'on Gravel, or the Kefar Yuval Travertine. 1t is built of two monomineral­

calcitic travertine facies (like the Kefar Yuval Travertine). 1ts appearance in the field is very

similar to that of the Kefar Yuval Travertine, and distinction between the two can only be

made geochemically (Heimann, 1985).

The age ofthe formation is Upper Pleistocene: its top, dated by C14, was determined as

25,000:I:800 yr (Heim~ 1985).

17

) 8. BASHAN GROUP (Pliocene-Quaternary

The Bashan Group (Mor, 1986) is built of five volcarllc units: the Cover Basalt

~) 1994 , the Eitar Basalt (a unit comprised in the Meshki Basalt of Mor ~ SchuIman, 1962) (

, emended by Mor ~ and the Golan Formation (Mor, 1973 ~ the Ortal Formation (Mor, 1986)

1986). The fifth and youngest formation (less than 0.1 m.y.) is the Leja Formation - El

Wa'ara Basalt of Dubertret (1954) - which is found in southem Syria. The formation

.) 1986 , 1973 ( members were determined by Mor .

-the Golan heights are generally of uniform composition (aIkaline מiThe volcarllc rocks

iolivine-basalt) with no possibility of distinguishing between one basalt unit and anotherמ

ce every unit מihand-samples, thin sections or simple geochemical analyses. However, s

the field and on aerial photographs, morphostratigraphic criteria can be מilooks different

applied, with limitations, to distinguish between them. The paleomagnetic criterion can also

. be utilized, but only to a limited extent

) the present division of the rock units (formations and members מiThe deciding criterion

the Bashan Group is chronostratigraphic. Accordingly, contemporaneous basalt flows are מi

areas מI. ascribed to the same mapping unit, providing they exhibit stratigraphic continuity

adjacent to dated sites, morpho-stratigraphic criteria are applied. Often, thick paleosols

separate between the units. An attempt to characterize volcarllc units geochemically was

. made by Weinstein (1992), yet his findings postdate the mapping

the scoria and tutf may accumulate to many tens of ~ thickness מiThe volcarllc units vary

meters in a Iimited area, as a result of repeated eruptions, and be completely absent in the

~ rest of the area. The lava spread out over a broad area, forming relatively thin basalt layers

. where it flowed through ancient, narrow channeIs, it is obviously much thicker

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) c 38.1ז. Cover Basalt (P

, the Lower GaIilee מiThe Cover Basalt is distributed over a very broad area: it is found

. the Golan heights, southem Syria and northem Jordan

the Har Ram lava מithe south, and מiIn the Golan heights it crops out over a wide area

. cone in the north

. Its type section, which is found in the Galilee between Nahal Issakhar (base coord

1971/2186) and Hirbet Jabul, is 150 m thick (Schulman, 1962). In the Golan the formation

thickens fi"om 55 m in Mevo Hama to 175 m near Qubet Qar'a (Michelson, 1972). The

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the flat, broad lava cones, of Giv'at Bene מiCover Basalt in the southem Golan originated

Yehuda, Rujm e-Zaki, Giv'at Bezeq, Giv'at Natur and Qubet Qar'a. Scoria and some tuff

. the Bene Yehuda Scoria Member) are also exposed in the first three cones (

Freund et al. (1965) note that the lower part of the Cover Basalt in the Galilee is of

the Golan heights מi, normal, and the upper part, of reverse magnetic polarity. However

.) 1984 only reverse magnetic polarity was found (Ron,

The radiogenic age of the Cover Basalt (Mor et al., 1990) was measured on 24 samples

the Golan. The earliest age, found at the base at Ne'ot Golan, was מitaken ftom eight sites

5.05 i:: 0.12 m.y. (the average ofthree samples). The latest average age, measured at the top

.). ofthe section, at Har Ram, was 3.71 :f: 0.18 m.y. (earlier measurement on map, 2.8 m.y

Thus the entire formation was built within approximately 1.34 m.y., during the Lower

.) 1996 ( . Pliocene. Post-mapping data is given in Heimann et. al

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,) 1994 ( The Eitar Basalt, which is a local member comprised in the Meshki Basa1t ofMor

the area ofTel Abu el Eitar. 1t yielded an age of מi, crops out in the southem Golan heights

which מi:J:0.20 m.y., which fal1s within the Upper Pliocene range of ages, the range 2.7ן

other basalt flows in Lebanon (Meshki), Upper Galilee (Dalton) and the Korazim plateau

Lebanon through מiRuman) fa11. The Meshki Basalt flowed ftom the area ofBad el Ahmar (

age ftom מithe ancient Hasbani channel to the Hula Va11ey (Mor, 1986). 1t ranges

cludes basalt flows and scoria ftom three מi2. 98:J:0.14 to 2.23:J:0.I0 m.y. The Dalton Basalt

sma11 cinder cones. 1t overlies the Dalton plateau (Mor et al., 1987) and ranges in age ftom

the Korazim מi2.6O:J:0.40 to 1.69:J:O.11 m.y. The Ruman Basalt is exposed at Tel Ruman

age ftom 2.5 m.y. to 2.0 m.y. (Heimann et מiplateau, where it probably originated. 1t ranges

.) 1990 al., 1987; Heimann and Steinitz, 1988b; Heimann et al., 1989; Heimann,

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8.3. Ortal Formation (Qf3o)

Following a short period during which no volcanic activity is known in the Golan, the

volcanism was rejuvenated; the resultant flows are found on the Golan plateau as well as in

the Rift.

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8.3.1. Dalwe Basalt (QJ3od)

The Dalwe Basalt was first described fTom the Ortal (formerly Dalwe) ridge at coord.

2210/2770. It covers broad areas in the central Golan heights and appears also in the north

and south.

In the southem part of the Golan heights it ranges in thickness fTom a few meters to tens

of meters; it overlies the Cover Basalt, with a thick paleosol separating between the two. In

Nahal Orevim it unconformably overlies the Bar Kokhba Formation and is more than 150 m

thick; in the "Alonne Bashan 2" borehole, 286 m of this basalt was penetrated without

reaching its base. Usually the unit is overlain by the Golan Formation basalts.

The sources of the Dalwe Basalt are a series of flat, broad, ellipsoid lava cones (see a1so

paragraph 8.3.2. Sheivan Scoria), whose long axes are orientated north-northwest (N16W),

and the line connecting their centers runs in a northwest (N47W) direction. The unit is built

of a great number of basalt f1ows, usually with paleosols between them, as, for example, in

Nahal Orevim and Nahal Zawitan. For all but the three middle flows in Nahal Orevim, the

magnetic polarity is reverse (Mor, 1973; Fogel, in Mor, 1986). The basalts fTom the lava

cones flowed mainly southwest, towards Lake Kinneret, over an average slope of 3 degrees.

The surface exposures of the Dalwe Basalt are very rugged compared to those of the

underlying Cover Basalt and the overlying Muweisse Basalt (Netser, 1982). Most of the

dolmens and megalith relicts of the Golan are densely concentrated on the Dalwe Basalt

exposures.

The age of the Dalwe Basalt was measured on 48 samples. Most were taken fTom

outcrops and one was from a core from the Alonne Bashan 2 drillhole. The age of the top of

the unit, (near the Fazra junction) is 0.70:1:0.19 m.y. The base of the section in Nahal

Orevim yielded an age of 1.58:1:0. 1 m. y., and that from the bottom of the Alonne Bashan 2

drillhole, 1.54:1:0.19 m.y. However, additional age measurements, made following

innovations in the analytical laboratory procedures after the maps were published, yielded

older ages, around 2 m.y.

8.3.2. Sheivan Scoria (Q<jos)

The Sheivan Scoria was first described from Tel Sheivan (coord. 1978/2809), which is the

largest of the units' s volcanic structures. Included in it are several cinder cones, and a1so

20

volcanic depressions (resulting ftom explosions of gas discharged under great pressure) and

ring structures.

The volcanic structures are eroded and less distinct than the younger Odem Scoria cones.

They are aligned in rows on top of the Dalwe Basalt lava cones, generally in the same

direction as the long axes of the elliptic lava cones. The prevailing lithology is reddish scoria

and agglutinate (Mor, 1973, 1986).

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) 8.3.3. Hasbani Basalt (QJ3oh

The Hasbani Basalt (Picard, 1963; Mor, 1986) originates in Mazra'at e Darajat in

Lebanon, apparently west of Kaft Halata; it is distributed in the Hasbani Valley and the

northem Hula Valley as far as Qiryat Shemone, over an area of about 450 sq. km. The most

. complete section, about 40 m thick (the base is not exposed), is in Nahal Hasbani (coord

2086/2941). The age ofthe Hasbani Basalt was measured on 25 samples taken ttom 8 sites

(Mor, 1986; Heimann, 1990). The oldest, 1.35M.46 m.y., is ttom the base of the exposed

0.04 m.y., ftom a site near Ma'yan :0.83ב , section in Nahal Hasbani, and the youngest

. Barukh

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8.3.4. Yarmouk Basalt (QJ3oy)

The Yarmouk Basalt (Noetling, 1886; Picard, 1935; emended by Michelson, 1972)

apparently derived ttom a volcanic source in Syria, and flowed through the Yarmouk gorge

towards the Jordan Rift. What remains of this basalt today are a just few terraces, 100-200

m above the present river level. The maximum thickness ofthe basalt is about 30 m, though

it is clear that this represents only part of its original thickness. The basalt unconfonnably

overlies the Eocene units of the Avedat Group. The magnetic polarity in its upper part in

nonnal.

In the Naharayim area there are several basalt outcrops - the Naharayim Basalt ofPicard

(1932). This basalt unconfonnably overlies the Ubeidiya Foramtion, interfingers with

pebbles of the Naharayim Fonnation, and is overlain unconfonnably by the Lisan marls.

According to Fogel (in Mor, 1985), its magnetic polarity is nonnal. Age detenninations

showed the Naharayim Basalt to be the same age as the Yarmouk Basalt, and it is evidently

the continuation of the latter within the Rift. The age of the Yarmouk Basalt was measured

on seven samples ftom two sites; the average age yielded for the top of the unit is

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0.17 m.y. (Mor, 1986). Another 10 dates were obtained by Heimann, (1990) fi"om 90.7 :כ

. their average age is 0.6 m.y ~ four t10ws ofthe Naharayim Basalt

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8.4. Golan Formation (Qf3g)

Included within the Golan Formation are eight members: three - the Muweisse Basalt, the

Odem Scoria and the 'En Ziwan Basalt, are widely distributed, whereas the Raqqad Basalt

(in the Yarmouk drainage system in southem Golan), the Avital Tuff, the Keramim Basalt,

the Berekhat Ram Tuff and the Sa'ar Basalt (in the northem Golan) occur only locally. ["IiiI

8.4.1. Muweisse Basalt (Qf3gm)

The Muwseisse Basalt, which was first described fi"om the area of the abandoned village

Muweisse (coord. 2205/2812), comprises a series ofbasalt t10ws unconformably overlying

the Dalwe Basalt. The basalt lavas flowed between ridges, mainly in a southwest direction,

and, in at least one place, reached as far as the Hula Valley (Nahal Hemdal, coord.

2108/2777).

Paleosols are found in places between the Dalwe Basalt and the overlying Muweisse

Basalt. The magnetic polarity of this unit is usually normal (Mor, 1973~ Fogel, in Mor,

1986). Brenner (1979) showed a difference between its trace element composition and that

ofthe Cover Basalt (and also between that ofthe 'En Ziwan Basalt).

The sources of the Muweisse Basalt are the cones of Har Odem, Har Bental, Har A vital,

and the Haziqa ridge, which are also the sources of the Odem Scoria and the 'En Ziwan

Basalt. The flows of the Muweisse Basalt form steps, each with a steep fi"ont and t1at t10w

surface which is covered by soi1 (for the most part also cultivated). At the end of the rainy

season many small springs issue fi"om the t10w fi"onts.

Netser (1982) noted a number of characteristics, such as the fi"acturing, weathering and

also the soi1 development, which enable distinguishing between the Muweisse and the

Dalwe Basalts.

The age of the Muweisse Basalt was measured on nine samples taken fi"om three sites~ the

average age calculated for the top ofthe unit is 0.33:1:0.07 m.y.

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. t found at the base of Har Keramim (coord iתThe Keramirn Basa1t is a local basa1t u

s ofBerekhat Ram.. It is exposed over an area of giמ the northem mar מi2229/2916) and a1so

. about 3 sq. km

t overlies sedimentary rocks and is overlain by the Berekhat Ram. Tuff; southwest uתi The

of Berekhat Ram. it is overlain by the Odem Scoria. Where its sources are, is not clear; they

the east. The Keramim מimay be buried beneath Har Keramim, or beneath Har Manfuha

a מithe Golan, is weathered and ftiable. It is ftactured מiBasalt, unlike the other basalts

woof and warp pattem, with hard ledges often appearing within it, and has a light

. bluish-gray, or reddish-gray to yellowish color

ger, 1983) containing many remnants מit there is a thick reddish pa1eosol (S uתi Within the

c age was eתi and artifacts of the Upper Acheulian culture (Goren-Inbar, 1985). Its radiog

determined by Feraud et a1. (1983) by the AIIAI method; the section below the pa1eosol is

) 1986 ( between 0.3 and 0.8 m.y., whereas the section above it is about 0.23::f:O.03 m.y. Mor

, g the KI AI method מius ~ gle site above the pa1eoso מiexamined eight samples taken ftom a s

. which yielded an average age ofO.25::1:0.06 m.y

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The Odem Scoria (after Har Odem, coord. 2208/2294) builds a group of pyroclastic

the eastem Golan heights, ftom Har Peres to מitwo rows מictures which are aligned stזu

Berekhat Ram., trending north-northwest (N17W). The pyroclasts generally include

agglomerates, breccia, volcanic bombs and lapilli, and some tuff. The materia1 is generally

unsorted and is coarsely bedded or not bedded at all; occasiona11y it appears as graded

bedding (e.g., at Har Peres and at Har Bental). Most ofthe cones are less than 100 m high;

t is the uתi but Har Benta1 and Har A vita1 reach a height of 200 m and more. Typica1 of this

which stands out ftom afar. The separation between ~ red-purple color of the covering so

ts predating it (Bene Yehuda and Sheivan) is based uתi the Odem Scoria and the two scoria

chiet1y on field relations. The fact that the cones are still very distinct and almost completely

preserve their original shape - despite the ftiableness of the rock building them and the high

precipitation in the area - shows they are of a young age, and their appearance on top ot: or

ts of the Golan F onnation points to an age younger than the base of this iתin between the u

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formation (0.36 m.y.). To date, two samples of scoria were dated: one f]-om Har BentaI

yielded an age ofO.26::1:0.03 m.y., and one trom the foot ofHar Peres - 0.33::1:0.17 m.y.

8.4.4. 'En Ziwan Basalt (Q(3ge)

The 'En Ziwan BasaIt (after Kibbutz 'En Ziwan, coord. 2248/2782), buiIds a number of

Iava cones in the northem part ofthe Golan (Har Odem, the Haziqa ridge, the Mahfi ridge).

It aIso comprises lavas which f10wed f]-om cinder cones in which the Odem Scoria is

exposed. These lavas, which f10wed downslope over the Muweisse or DaIwe basaIts, have a

distinct rugged surface. The magnetic polarity of the 'En Ziwan BasaIt is generaIly highly

normaI.

The age of the 'En Ziwan basaIt was measured on six samples fTom two sites; the average

age obtained in Bab el Hawa is 0.32::1:0.14 m.y. and that near Mas'ada, 0.12::1:0.02 m.y.

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8.4.5. Avital TutT (Q'tga)

The AvitaI Tuff is a pyroclastic unit covering Har AvitaI (coord. 2245/2793) and the

Quneitra plain. It is built of lapilli, fine andcoarse tuff, some basaIt fi"agments and rounded

scoria, and likewise, volcanic bombs and clay horizons.

Har A vitaI is a complex volcanic structure trom which large quantities of tuff were

ejected, followed by the collapse of its center. The Tuff overlies the Odem Scoria, with a

graduaI transition (sometimes with interfingering) between them, or it overlies the

Muweisse BasaIt with a thick plaeosol separating between them. In boreholes in the

southeastem margins of the mountain, the tuff is maximaIly 36 m thick (Soudry and

Bogoch, 1971); it apparently becomes thicker to the northwest. Eastwards the unit

decreases in thickness to 6-8 m in the center of the Quneitra plain, and further east it

disappears completely.

Mor (1973) distinguished two facies in the AvitaI Tuff: the Merom Golan facies, which is

built mainly oflapiIli, tuff and bombs up to 2 m in size, and of a few wind-laid clay horizons;

and that found in the Quneitra plain, which is buiIt of lapil1i, tuff without bombs, and thicker

clay horizons which contain plant remains. The sorting and bedding are good, pointing to

deposition in a lake or swamp environment.

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8.4.6. Raqqad Basalt (Qf3gr)

The Raqqad Basalt (Noetling, 1886~ Blanckenhom, 1914~ Picard, 1932~ :Michelson, 1972)

flowed from the Golan in Syria, southward to the Raqqad canyon, and falling into it,

continued to flow through it and the Yannouk to the Rift Valley (Mor, 1989~ Mor et. al.,

1989). 1t builds a row oflow terraces that are 30-60 m above the present channellevel and

are better preserved than those of the Yannouk Basalt. 1t is, at maximum, 40 m thick

(Michelson, 1972), though it is clear that part of it was eroded by the river. 1t

unconformably overlies Eocene units ofthe Avedat Group.

At Tel Dover, at the mouth ofthe Yannouk River, the Raqqad Basalt is faulted against

the Lisan marIs.

The age of the Raqqed Basalt was measured on twelve samples ftom four sites~ the ages

obtained range ftom 0.48 to 0.37 m.y.

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1.5 The Berekhat Ram Tuffis found around Berekhat Ram (coord. 2218/2932) and in a

sq. km. area within a small valley east of it. 1t is built of black, coarse, massively-bedded

tuff, or of layers of less-coarse, variegated tuff altemating with thin layers of clay. There are

, scoria bombs and xenoIiths (mainly ultramafic minerals and metamorphic rocks

Mittlefeh1dt, 1982, 1983) as well. 1n boreholes around and within the pooI, a number ofthin

.) 1971 , basalt flows were found interfingering with the tuff(Kidron

to the west it ~ To the southeast the tuff unconformably overlies the sedimentary rocks

overlies the Odem Scoria and to the east and north, the Keramim Basalt. Close to the

viUage ofMas'ada the tuffis overlain by the Sa'ar Basalt, with a thick paleosol separating

is ~ between them. The tuff unit in the subsurface, measured in boreholes within the poo

. between 34 and 60 m thick, thinning from the center of the pool to its margins

The source of the tuff was evidently an ancient volcano which erupted where Berekhat

Ram is found today (Mor, 1986). After the tuff was ejected, the entire center collapsed,

) falling inward. The tuff ranges in age between 0.25 m.y. (the age of the Keramim Basalt

.) and 0.14 m.y. (the age ofthe age ofthe Sa'ar Basalt

(111)

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8.4.8. Sa'ar Basalt (Q(Jgs)

A number of flows of the Sa'ar Basalt were extruded ftom an unknown source and

flowed through the gorge ofNahal Sa'ar, which separates between Mount Hermon and the

Golan heights, as far as the Banyas region.

The area covered by the Sa'ar Basalt ranges between 100 and 1000 m in width and is

about 8 km Iong. In the Sa'ar gorge the basalt overlies stream graveIs, which in tum overlie

sedimentary rocks on the northem side of the gorge and the 'En Ziwan BasaIt on the

southem side.

Age measurements performed on four samples of the Sa'ar BasaIt taken ftom two sites

yielded an average age ofO.14::1:0.007 m.y.

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9. UNDIVIDED BASALT (Q (J)

Since the morphological criteria that help to determine to which of the various members

the basalt should be ascribed to are blurred or absent in the area of the faults in the westem

Golan heights, at this stage aIl the basaIts in this area are included as a single unit under the

name ''Undivided Basalts".

It may reasonably be assumed that the majority of these outcrops are of the Dalwe BasaIt,

and a few may be of the Muweisse and the 'En Ziwan basaIts. Indeed, ages determined by

Heimann since the completion of the maps support this assumption.

!!!'II!

) 10. ALLUVIUM, including Soils (AI

places, quite a מI. The aIluvium covers broad areas on the plateau and in the Hula Valley

thick soil profile develops on the basalts. The soil is clayey and generally contains basalt

. ftagments

in the river valleys they consist of pebbles ~ In the Hula VaIley the soils are generally clayey

, and boulders. (F or more on the soils of the Golm heights, their composition and structure

.) 1973 , see Dan and Singer

GEOLOGICALSTRUCTURE

The geological structure of the area is inherently different in the two physiographic

regions noted: the mountainous Hermon in the north of the mapping area is an anticlinaI

26

structure; the Golan heights is a volcanic plateau under which an earlier geologic structure

is hidden.

CLINE 1ח. THE HERMON AN

, The Hermon is a NE-SW trending anticlinal structure, 36 km long and 14 km wide

extending over some 500 sq. km. The culmination of the anticline is in the Arne area in

Syria; rocks of the Lower Jurassic Inmar Formation crop out there. Its fIanks are

asymmetric; the southeastem fIank is the steeper, with dips reaching up to 50 degrees in the

Har Odem quadrangle. The northwestem flank is more moderate, with dips ranging

. between 20 and 30 degrees

. The faults, which generally parallel the axis of the structure, divide it into several blocks

The amount and direction ofthe throws ofthese faults are difficult to discem because ofthe

thick uniform carbonate section of the Hermon F ormation, which builds most of the

structure. The existence of a left lateral displacement on the Nahal Si'on fault (the segment

of the Rashaya fault in the Har Odem quadrangle) was argued by Freund (1980) and

Heimann (1985). The Barhata Valley graben developed between the Si'on fault and the

continuation of the Rashaya fault (Heiman et al., 1989). The Newe Ativ graben is also

found within the Har Odem mapping area. In it Shimron (1988) found a volcanic complex

built of polymictic volcanic breccias with carbonate blocks :&om the country rock. Shimron

considers at least part ofthe Newe Ativ graben a collapsed volcanic caldera that was active

. during the volcanic phase ofthe Lower Cretaceous

The Hermon is part of the Syrian Arc, a series of folded mountains which extends :&om

the Sinai Peninsula through Israel to the Palmyra Plateau in syria. The generally accepted

time of its formation is :&om the Cretaceous to the early Tertiary (picard, 1943). Freund

1980), however, proposed that like Mount Lebanon, the formation of Mount Hermon is (

connected to a strike-slip along the Dead Sea Rift. Mimran et al. (1985) found indications

of possible embryonic folding in the margins of Mount Hermon already during the

the absence of Mount Scopus and A vedat group rocks adjacent to the flanks מI. Paleocene

. ofthe Hermon structure, the beginning offolding ofthe Hermon is difficult to establish

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2. THE GEOLOGICAL STRUCTURE BENEA TH THE VOLCANIC PLA TEAU

Eocene to Neogene rocks in the southem Golan heights are found in a broad depression

extending between the Hermon anticline in the north and the Ajlun anticline in the south.

I~'

27

Because of the basalt cover, it is difficult to know if this is a continuous depression or if it is

divided into several structures, as implied ftom a geoelectric survey (Michelson, 1972). In

the northem Golan the Shamir Kipuka outcrops and a few other small "windows" (Mimran

et al., 1985) display two unconformities, one at the base of the Ghareb Fonnation and the

other at the base ofthe Taqiye Fonnation. These are evidence oflocal post-Campanian pre­

Maastrichtian and Paleocene tectonic activity. Depth to the Middle Jurassic strata in the

central plateau area was estimated by May and Shulman (1989) at about 2200 m on the

basis of seismic pro:files.

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3. FAULTING

. The Golan heights are bounded in the west by the large faults ofthe Rift, which trend NS

,) Three major faults, the Si'on, Shamir (Har Odem sheet) and Sheikh Ali (Gamla sheet

s dip giת branch off them in a general NNE direction. The strata exposed at the rift mar

.) 1996 strongly, in places, towards the eastem NS faults ofthe Rift (Michelson, 1979; Sneh,

Seismic profiles across the main NS transfonn ftom the Korazim plateau to the Golan

heights were studied by Rotstein and Bartov (1989). The exact vertical throw ofthe main

Rift faults east of the Hula Valley is difficult to measure because of the absence of clear

guide horizons within the basalt. Ar/ Ar ages of basalts ftom the Notera 3 borehole drilled in

the Hula segment of the Rift indicate (Heimann and Steinitz, 1988a, 1989) that rocks of the

Dalwe Basalt, which also crop out at the westem margins of the Golan, were encountered

in the borehole between 500 and 900 m, and those of the Cover Basalt, between 1657 and

2418 m. In a number of places young volcanic formations cover the faults that were active

: on older basalts; this enables separating the faults into two groups

a) Faults which are post-Ortal Formation (whose age is younger than 0.6 m.y., though it

is likely that they were active even before this) and are covered by basalt flows of the Golan

Formation, i.e., the northem part of the Sheikh Ali Fault, the Shamir Fault and the Ein-el

.) 1973 , Warda faults (smal1 sinistral faults according to Michelson, 1972 and Mor

b) F aults that postdate the Golan F onnation (whose age is younger than 0.1 m. y., though

most likely they were also active earlier), i.e., the Si'on Fault, the faults in the Nahal

. Hemdal area and the Rift faults in the Shamir-Banyas area

F'I I

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28 r 4. THE VOLCANIC ALIGNMENTS

. The volcanic cones which relate to different formarions are aligned in different directions

The arrangement in elongated strips hint at a connection to lineaments of tectonic

significance possibly deep in the subsurface. The lava cones of the Cover Basalt in the

southem Golan heights are not oriented along any line whatsoever. The three lava cones of

the Ortal Formation (Dalwe, Hakim and Sindian, each with 2-3 smal1 negative structures on

top) together with several cinder cones (such as Tel Sheivan and Tel Mughayir, and also Tel

Kudna, Tel el Asbakh and Tel Mahir just past the border) form a belt 3 krn wide, trending

. N47W, extending ftom Tel Kudna in the southeast to Tel Sheivan in the northwest

The Golan Formation builds most ofthe volcanic structures in the Golan. Included among

these are four large lava cones (Har Odem, the Haziqa ridge, the Mahfi ridge and Har

Peres), two calderas (Har Avital and Berekhat Ram) and about 60 cinder cones and

composite cones of varied types and sizes. They are all arranged in a belt about 7 km wide

W, fTom the Qal'aa ךates slightly fTom it) trending N1 ~ except for Har Shipon which .de (

cones in the south-southeast to Berekhat Ram in the north-northwest. This is also the

dominant orientation of the depressions and the craters on the sides of the cinder cones in

. this formation

The belt can be divided into two parallel structural alignments, the eastern, running

through the Qal'aa cones, Har Peres, the Haziqa, the Rasaniya and the Mahfi ridges, Har

Hermonit, Har Warda, Har Keramim and Berekhat Ram - and the western alignment, that

begins at Giv'at Oreha and passes through the Hushniyya and Ramtaniyya cones, the

Yosifon, Avital, Bental and Bar'on mountains up to Har Odem. Each strip is 2-3 krn wide

. with a distance of 2 km separatiang between them

Twenty-three djubas (djuba - a local Arabic name for a round-shaped volcanic

depression), several tens to 300 m in diameter, and up to 100 m deep, fal1 within another

belt that is 4 km wide and trends N43E ftom the Shamir Kipuka in the southwest to the

djuba near Berekhat Ram. There are additional djubas in line with this same belt across the

border as far as Tel Hadar. This belt runs parallel to two adjacent principal faults, the Si'on

and the Shamir. Mor (1986) assumes that the djubas are the results of volcanic gas

eruptions along a buried tectonic lineament and that chronologically, they belong to the last

. volcanic phase that formed the "small Leja" in southwest Syria

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29

GEOLOGICAL HISTORY

During the Middle Jurassic the area was a part of a huge marine depositional basin which

extended over the entire Levant (Goldberg, 1980). This basin was shallow enough for minor

-tectonic movements to result in changes in the environments of deposition; i.e., fi'om a low

energy, quiet marine regime to one of high energy in which shoals developed. These

conditions, which prevailed throughout most of the Bathonian and the Lower Callovian

Hermon Fm.), changed towards the Upper Cal1ovian-Oxfordian (Kidod Fm.), the basin (

became closed and water circulation limited. In the Middle and Upper Oxfordian (the Beer

. Sheva and Haluza fins.) open marine, and general1y high energy conditions retumed

Basalt flows related to the Lower Cretaceous volcanic phase covered the progressively

the next stage the Hatira sandstones מI. eroded relief of the Haluza and Beer Sheva rocks

were deposited within a very wide basin, covering the whole of northem Israel and southem

.) 1965 , Lebanon (Karcz

The Ein-el-Asad (the ''Blanche'' clifi) and Kati'h formations constitute the first

transgression-regression cycle ofthe Judea Group. Sediments ofthe first formation reflect a

. shallow marine environment of deposition; the sands above it point to further shallowing

The new transgressive cycle began in the Albian and continued to the Campanian. During

this period sediments of the Mas'ada, Yagur, Deir Hanna, Sakhnin, Bina and Menuha

. formations were deposited

From the end of the Campanian the area was affected by several tectonic movements

(Mimran et al., 1985), the first of which was responsible for the removal of the upper part

of the Menuha Formation (Lower Campanian) in several places, and for removing the

Menuha, Bina, Sakhnin, and part of Deir Hanna formations in the Shamir Kipuka. The

marine regime was renewed in the Maastrichtian and is manifested by the deposition of

sediments of the Ghareb F ormation. There are no sediments representing the period ftom

the end of the Maastrichtian to the beginning of the Lower Eocene; there may have been a

. break in sedimentation, possibly as a result of an uplift in the area

the northem parts of the מI. The marine sedimentation was renewed in the Eocene

mapping area marls ofthe Taqiye Formation were deposited, followed by limestones, chalks

and cherts of the Adulam and Bar Kokhba formations. To the south the extensive Eocene

transgression resulted in the deposition of several hundred meters of limestone, chalk and

chert sediments - the Adulam and Maresha formations. The uplift at the end of the Middle

jח!iii!

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30 fRUן

Eocene caused a regression of the sea and the formation of the anticlines and synclines in

the area. In the Upper Eocene and Oligocene, chalks, dolomites and biogenic limestones of

the Fiq and Susita formations were deposited during a marine transgression, which was

apparently connected with the Persian Gulf

Renewed folding and uplift in the Neogene ended this transgression and a regime of

erosion and sedimentation in in1and continental basins began. The fluvial conglomerates and

sands and the limnic limestones of the En Gev and Hordos formations reflect this regime.

During this period a number of volcanic eruptions took place in the area. Volcanic activity

in the area continued in Upper Miocene as well.

Prior to the main phase of volcanism in the Golan which took place during the Plio­

Pleistocene, a short-lived marine transgression reached the southem Golan heights, filling

the depressions and depositing marls and biogenic limestones (Bira Fm.). A number of

shallow lakes were left in the area after the connection to the Mediterranean Sea was cut

off, and calcareous sandstones, marls and limetstones (Gesher Fm.) were deposited in them~

interfingering are several basalt flows.

We have no information enabling evaluating the geological history of the period fi"om the

Upper Eocene to the Pliocene in the mapping area in the central Golan. It is possible that

there are sediments ofthis period under the young Plio-Pleistocene basalts. Both marine and

continental sediments fi"om the Upper Eocene-to-Pliocene period crop out in the southem

part ofthe Golan heights.

In the Lower Pliocene a period of intensive volcanism began, which continued

intermittently to the Holocene; during this period the Bashan Group was built.

During the first volcanic stage (fi"om about 5.1 to 3.5 m.y., Mor, 1993; Heiman, et al.,

1996) the Cover Basalt spread over the entire area from Har HaDruzim to the Yizre'el

Valley, covering the existing relief.

During the next volcanic stage, (from about 2.9 to 1.7 m.y.) basalts erupted and flowed

both in the Ri:ft and around it. Old flows are recognized in Lebanon (Meshki), in Upper

Galilee (Dalton), in the Korazim plateau (Ruman) and in the southem Golan heights (Eitar).

Subsidence ofthe Jordan Rift continued along with the development ofits drainage system.

Younger flows (Dalwe basalts, from about 1.6 to 0.7 m.y.) erupted on the Golan heights

and flowed to the Rift through the existing drainage network. North of the Hula Valley,

within the Ri:ft, the Hasbani basalts erupted and flowed as far as Qiryat Shemona. The

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31 r-

Yarmouk BasaIt, which originated in southem Syria, flowed through the Yarmouk gorge to

. the Naharayim area in the Rift VaIley

In the following volcanic phase (fi"om about 0.40 to 0.10 m.y.) the Golan Formation was

, g through the DaIwe BasaIt מiformed. Its flows streamed within the drainage network cutt

towards the Hula Valley. The Raqqad BasaIt flowed through the Raqqad and Yarmouk

gorges to the Jordan VaIley. Many cinder cones formed on the Golan plateau, and in two of

. the largest, Berekhat Ram and Har AvitaI, coIlapse caIderas formed

In the last volcanic phase (0.062 m.y., Heiman et aI., 1993) the EI-Wa'ara Basalt (the

. small Leja") was formed in southwestem Syria "

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ECONOMIC GEOLOGY i L

. The main natural resources ofthe Golan are building stones and curative mineraI springs

The basalt is in demand for building and industrial purposes; large massive blocks are

processed, cut and polished for tombstones, commemorative monuments and decorative

plates. Basalt pebbles are quarried for the production of various components for the

." building industry, such as building blocks, decorative floor tiles, mosaics and "rock wool

In effect, the basalt is unlimited in quantity. The principle quarries are located near Ka:fr

. Nafah and in the alluvial fan ofNahal Daliyyot

The scoria and the tuff are suitable for the light cement industry, insulation sheeting, hot

houses, filling for planters and window boxes, and also as coating material for roads. These

materials are quarried at Har Peres and at Har Bental (Yanai et al., 1989) and at Har

the מiHermonit. Chalk and limestone rocks suitable for cement production are found

Maresha Formation exposed in the southem Golan along Nahal Samakh, Nahal En Gev and

the Yarmouk River. Loose sand for building and paving purposes is supplied by the En Gev

. Sands. An operatiang quarry is found next to Kibbutz En Gev

the Hermon, the מiExcept for the Banyas and Dan springs, whose sources are in the karst

springs in the Golan heights are medium to small with seasonal fluctuations, and water

idrillholes in the basalts were for the most part dry; therefore floodwaters are collectedמ

artificial reservoirs on the plateau. Berekhat Ra.m. which collects the waters of the nearby

Nahal Sa'ar, serves as a perennial reservoir in the north. The Hammat Gader springs are fed

. the Gil'ad plateau in Jordan מiby the Cenomanian-Turonian aquifer whose recharge area is

. A spa and bathing center have been developed around the OOt springs at Hammat Gader

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32

ACKNOWLEDGMENTS

We thank Y. Bartov for his consructive comments on the manuscript, N. Shragai for the

preparation of the figure and B. Katz for editing the report.

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~ I

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r iiII

rו

,.

•

•

•

34

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i i

lI!Ii!

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r ,.

f!III

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l1i'JI'!I

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f!i!I\'I

[i1!II

35

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~

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37

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r-

LITHOSז RATIGRAPHYה Iגרפ Iסטרט Iת Iל;.: :;

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Figure 1. The stratigraphic column of units exposed in the Golan heights.

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הגולושללגיאולוגיההערות

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הערוציםמצוקיאתבונותטקייהחבורתשלהתזותוניםוהזולקיםבעדתזובורתיחידות

הרמה.בדרוםהחותרים

יבשתייםדקות,שכבותמטפרלמעטטקייה,חבורתשלמיוקו,מגילהעליונים,החלקים

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ופירוקלסטים.בדלותכיללות

לרמה.ממערבבבקעהמלזויםזובורתמשקעיהצטבריבמקביל,

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הלאןמיןתהתשתיןתמשרד

הגיאןלןגיהמכןו 30ישראלמלכירח'

ישראל , 95501ירןשלים

Te [ .. 972-2-5314211טל. Fax . 972-2-5380688 .פקס

Geological Survey of Israel istry of National Infrastructll1"eS ךThe Mil

. 30 Malkhe Israel St ] 95501 Jel"Usa]em, Israe