From: Bill Brown Sent: Monday, November 13, 2017 4:47 PM To: Sidney Hill Subject: Comments on the Proposed Sandoval County Oil and Gas Ordinance Attachments: Sandoval county oil and gas comments WJB.pdf

Here are my comments Thanks Bill Brown

1 November 13, 2017 [email protected]

To: Attention: Sandoval County Commission Sandoval County, New Mexico

From: William Brown, P.G. 15 Snow Peak Road Placitas, New Mexico 87043

RE: Comments on the Proposed Sandoval County Oil and Gas Ordinance

Introduction The recently proposed “Stoddard Ordinance” in its current form poses a potentially serious threat to the long-term drinking water supply for the citizens of Sandoval County and potentially surrounding counties, pueblos, and municipalities, including the City of Albuquerque, the City Rio Rancho, and the Town of Bernalillo.

As part of the Comprehensive Zoning Ordinance of the Sandoval County, NM " SECTION 2. PURPOSE. “The provisions of this Ordinance are designed to promote health and the general welfare of the County; to secure safety from fire, flood, and other dangers; to protect local water resources; to facilitate adequate provisions for transportation, water and wastewater systems, schools, parks and other community requirements; to conserve the value of property; and to provide for the compatible development of land and other natural resources in Sandoval County."

The Stoddard Ordinance does not adequately meet the stated purposes of the Zoning Ordinance.

Hydrogeologic Setting

Sandoval County straddles several major geologic provinces including the San Juan Basin on the west and the Rio Grande Rift in the east. The San Juan basin is characterized by a broad depression with a relatively simple geologic environment.

The attached Figures 1 and 2 highlight the geologic setting in the eastern and more densely populated portions of the County. The Rio Grande Rift is characterized by numerous north-south trending normal faults which have resulted in the sediment infilled Rio Grande basin bounded by the uplifted Sandia mountains to the east. Tertiary and Quaternary basin fill sediments (shown in orange and brown on the attached maps), are the primary source of the Santa Fe aquifer. This aquifer provides drinking water for over half a million people in Sandoval, Bernalillo, and Valencia Counties. Proposed oil and gas exploration would penetrate these shallower aquifer zones and extend into the deeper Mesozoic and Paleozoic bedrock formations (shown in blues and greens on Figures 1 and 2). These underlying bedrock zones would likely be “fracked” as part of the oil and gas exploration/production well drilling process.

Potential Threats to Water Supplies

As can be seen on Figures 1 and 2, numerous faults are present in the vicinity of Bernalillo and Placitas areas. Implementation of Fracking in the proximity of these complicated and extensive fault zones poses a threat to overlying groundwater zones. Because of the highly complex large-scale nature of faulting in the area, the effects of fracking (and subsequent grouting) cannot be fully predicted. Horizontal fracking of bedrock adjacent to faults can result in facilitated migration of hydrocarbon contaminants (both oil and gas) along the fault zones to overlying groundwater zones. It should be noted that only the large-scale faults are shown on Figures 1 and 2; numerous smaller faults and fractures are present in the subsurface which are not shown on the maps/cross sections which further complicate the hydrogeology of the area.

Aquifer sensitivity to oil and gas production in the County generally increases from west to east. This is especially true in the vicinity of Placitas. Faulting in the Placitas area has also juxtaposed Mesozoic and Paleozoic (targets for oil-gas exploration) geologic formations against younger Tertiary and Quaternary Santa Fe aquifer formations. Fracking in these areas is even more problematic and potentially threatening to the areas water supply.

Conclusions

Oil and gas exploration and production is not an exact science and many things can go wrong during drilling, fracking, and grouting processes in complex geologic environments. This has been documented at numerous locations throughout the United States.

The current rush to approve what is a short-sighted and flawed policy towards oil and gas production in Sandoval County oversimplifies a complex problem and ignores the long-term needs of the Citizens of Sandoval County. The County Planning and Zoning Director does not currently have the expertise or the resources to make decisions which may drastically affect the long-term water supply for thousands of people.

At a minimum, Sandoval County should specify wellhead protection areas limiting or preventing oil and gas production within portions of the County based on aquifer sensitivity and land use. This is especially true in the eastern portions of the County and Placitas in particular due to its highly complex geology and potential aquifer sensitivity. No other water supply is available to the residents and municipalities in these critically sensitive areas. Historically, Mitigation of oil-gas exploration contaminants to drinking water aquifers is cost-prohibitive and generally impractical. Long-term litigations are usually the result.

Implementation of a more comprehensive approach to oil and gas exploration in Sandoval County can effectively mitigate these potential problems.

William Brown, P.G. Hydrogeologist Placitas, NM

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(LOMA MACHETE) (LOMA

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¥ 14 Qpo ¥

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l QTsa P8 ¥ 56 ¥ 18 Qpy

40 AM l QTsp ¥

¥ ¥ ¥

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l 8 ¥

l ¥ 8 65 Kd Pa ¥ ¥

l ¥ Jm ¥

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af ¥ 40 27 36 ¥ 24 Ma

¥ 28

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¥ ¥ 40 ¥ ¥ l Qpm ¥ 25 Pa 39

¥ 2 ¥ Qpo2 62 Lomos syncline ¥ ¥ 14 RG61275 ¥ ¥ ¥ 08

¥ 22 ¥ 19 ˛s ¥

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• 27 ¥

Qpo 15 ¥ ¥ Ma

4 3 45 Kmf ¥ ¥ 2 ¥ ¥ ¥

¥ Qca 25 18

¥ Qss 32 ¥ ¥ ¥ ¥

Qay 45 • 24

Kmf ¥ ¥

¥ ¥ W ¥ ¥ Kd ¥

RANCHO l Qay Jm

. Qpm2 l

¥ ¥

¥ 18

¥ ¥

l 70 28 ¥¥ ¥ ¥ ¥

¥ ˛m 30 ¥

¥ Khd Qca Jm ¥ 13 Qpo2 ¥ l Qre 35 25 ¥ ¥ Jt

l Qss e

¥

¥

Anticline—Trace of axial plane showing direction of plunge; dashed where approximately located, dotted where Qpo Qay ¥ ¥ 26

¥ l 2 Kd Jt Xr

¥ ¥ OF

daf ¥ Jm Je ¥ 47 5 ¥ 25 Pa 14 Km ¥ ¥

BERNALILLO ¥ s 10

¥ RG52453 QTsp u ¥ 45 ¥

Qam 2 cs Kmf ¥

¥ ¥ ¥ 25 af ¥

QTsa ¥ 55 30 Jt ¥ 14 Pa Ma ¥ ¥ ¥ ¥ Qay

concealed, queried where inferred af ¥ Je 57 t ¥ ¥

l ¥

¥ ¥

l

42¥

Qpm2 ¥ ¥ Je Jt 43 35 ¥ 6 l ¥ 35 39 Qpm 57 ¥ 37

¥ ¥

l 2a 50 5 ¥ ¥ ¥

08 ¥ 10 QTsp cs 63 ¥ Ma ˛s

QToc(?) ¥

RG64436 ¥ 55 Je ¥ 77 QToc(?) ¥ Khd ¥ Kml 11

QTob ¥ ¥ 40

Qss Kd ¥ 22 44

Qpo ¥

Qrd? l 1 ¥ 38 PLACITAS 32

¥ L ¥ Jm ¥ l ¥ ¥ 58

¥ ¥ D ¥ 37 Qss

¥ ¥ Je QHa U ¥

Qre ¥ 25 Qpo 26

Syncline—Trace of axial plane showing direction of plunge; dashed where approximately located, dotted where ¥ 27

2 ¥

¥ ¥ 32 80

¥

l 17 40 ¥

Qay ¥ a

¥ 45 Kmf l ¥

QHa BWWTS ¥ ¥ ˛m 17 ¥ l l Kd ¥ ¥ 7 30 Kmf ¥ Qpo 7

¥ QTsp ¥ 33 32 Kd 35 ¥ 2 Xr ¥ ¥ Jm

cs 30 s ¥

¥ ¥ ¥ concealed, queried where inferred ¥ 45 ¥

¥ ¥ ¥ 11

l ¥ ¥ ¥

¥

¥ Qae ¥ 25

2 ¥ ¥ 25 16 Ma

¥ Je Qpo

4 ¥ Kmf ¥ 31 2 ¥ Pa ¥

l 27

¥ Qca ¥ ¥

3 Qca 36 ¥ ˇcp

¥ ¥ ¥ ¥ ¥ ˛s

¥ Qpm1 Qpy 40 Kml 5

¥ 35 Jt

¥ ¥ Qpo

l ¥ QTob Qam ¥ 2

l ¥ Qpo3 Jm ¥ l ¥ Qpo

¥ ¥ ¥ 23 l 2 ¥ l Km ¥ QTsp Pa

l QTob ¥ cs ¥ l 35

Qrl ¥ ¥ Je Jt

Monocline with anticlinal bend—Trace of axial plane; short arrow on steeper bend; dashed where approximately Qrl ¥ ¥ 23 21 88

Qam Qca ¥ 23 ¥ ¥

7 ¥ ¥ 35 ¥ QTob? ¥

¥ ¥ 72 A' ¥

QTob ¥ ¥ ¥ Qay Qpo

¥ ¥ 7 ¥ Kd 25 19 16 2H ¥ ¥ ¥

¥ QTsa ¥ ¥ ¥ ¥¥ 19 Qss Xr

Qpo ¥ 20 22 ¥ 23 10 l Je ¥ ¥ 1 ¥ ¥

Qrl Qss ¥ Ma 45

located, dotted where concealed, queried where inferred ¥ 6

¥ ¥ 25 35 Qpo 69 Qca¥

¥ ¥ 1 20 ¥

¥

QTob ¥ ¥ ¥ 8 75 u

¥ daf ¥ Qpo Qay 15 ¥ 3 QHa

¥ QTsp c Jm ¥ 15 ¥ 48 Qss ¥ ¥ ¥

Kd ¥ Qpo1 l ¥ ¥ Qpo

¥ QHa QHa ¥ ¥ 3 80 50 ¥ e l ¥

QHa QHa ¥ ¥ Jm Qay 35 ¥ Qrl l Qrp 10 35 Kd Jm ¥ Jm Qpo1 42 Qpo 37 ¥ Tsla ¥ ¥ 30 10 1 43 Pa AM ¥ ¥ ¥ 40 r

Monocline with synclinal bend—Trace of axial plane; short arrow on steeper bend; dashed where approximately l ¥ QTsp cs ¥af¥ 35 ¥ Qpo3 27 l ¥

¥ 21 ¥ t ¥ Qpo l ¥ ¥ 1 ¥ 24 ˇcp 39 ¥ ¥

¥ ¥ Jm t ˇc ˇcp Qpo 07

¥ 30 1 a 60 QHa QTsp ¥ Jt

¥ ¥ Qrd? ¥ Qre c Kd Qpo l 36 1 ¥ 17 ¥ ¥¥ Jm Qpo located, dotted where concealed, queried where inferred Qae ¥ ¥ ¥ ¥ 3 ¥ 20 Pa 48 30 s ¥

¥ Qpo u ¥ Qpo

1 44 3 Qpo Suela fault

¥ ¥ ˇcp 1 2 ¥ ¥

l ¥¥ Qay 24 20 ¥ Qay Qao l Qam 30 Qpo1 a 37 ¥ l ¥

¥ Qss ¥ ¥ 25 20 ¥ QHa Qay Jt ¥ Qrl ¥ 19 40 ¥ ¥ ¥ Tsla 50

Qay 22 f A ¥ Qpo1 ¥ 10 ¥ ˇcp ¥ ¥ 25 ¥

Qay ¥ 25 ¥ Qpo ¥ 1 ¥ QHa ¥ ¥ 58 23

Qay Qpo3 ¥ 17ˇz ¥ Qss Breccia or gouge zones ¥ 33 f ¥ ¥ Jt 30 ¥ g

Qrl ? ¥ ¥ Qay 18 40 Je Qay ¥ Qay ˇcp a 50 l l

¥ 5 45 20 ¥ ¥ Qpo 40 zone ¥ ¥ 1 ¥ u

QTob Qpo ¥ 35 Qss ¥

o

3 27 ¥ ¥ ¥ u ¥

39 l Kml Jm 50 l AM ¥ ¥ Tsla

Qrl ¥ QTsp cs 12 15 l ¥

07 l Qa y ¥ ¥ 15 Jm 45 a 20 16 35 ¥ ¥ 18 ˛m

Qpo ¥ 3 Qpo ˇc 55 40 ¥ 30 Jt l Qca 30 l 20 3 ¥ 25 Slickensides on fault ¥ 23 ¥ 10 45 32 3 QTsa Qpm1 10 ¥ 16 ¥ Qpo2 ¥ 36 t

QTspcs 25 ¥ Qpo1 31 Qpo¥ 80 af 28 a ¥ Jm ¥ ¥ QHa ¥ ¥ Qpo 22 ¥ 45 ¥

Qpm2 1 15 23 ¥ ¥ Z 20 28

Tsla 26 ¥ ¥ ¥

Qay S Qpo1 ¥ ¥ ¥¥ ˇm 27 ˇm 60 l Qrpr 35 Je ¥ b

¥ ¥ 30 ¥ 15

Qre Qpo 25 ¥ ¥

l Qpy 3 ¥ Pa 6 ¥ 30 l E 22 ˇcp 36 a 46 ¥ I ˇcp ˇz Tsla ¥ ¥ ¥ ˇm 7 a Qca ¥ ¥ ¥ ¥ QHa l Strike and dip of bedding, horizontal bedding QTob Qam QHa 35 34 ¥

l C 10 25 r Qca ¥ ¥ 10 Qay Kml Qpo Qpo ¥ Qss Ps ¥ ¥ Qpm ¥ 3 3 ¥

¥ QHa 2b Qpm 25 65

Qae 2a ¥ ¥ 30 ¥ ¥ 44 Qss c ¥ A C

¥ ˇz ¥ 37 ¥

¥ ˇcp 12

¥ ¥ ¥ ¥ 24 Pa 70 ¥ ¥ F ¥

¥ ¥ a Ps¥

40 50 Qam 50 19 ¥ 14 ¥ 20 Qss ¥ Qca ¥

l ¥ ¥ Pa ¥

¥

l Qpm2 O ¥ ¥ ¥ Qss ¥ ¥ l Qay ¥ QHa QTob Qam Je Qpo1 Qca ¥ QHa ¥ 20 73 ¥ ¥ 38

Strike and dip of overturned bedding—ball indicates top of beds known from sedimentary structures . H ¥ 8 28 Ps ¥ Qay 88

¥

¥ Qpo ¥

1 ¥ Pg Qca ¥

¥ ¥

QHa ERRACES Ps ¥ ¥ Jt ¥ ¥ T ¥ 25 ¥ Qca ¥ Qay ˇcp 80 12 Qrl I Qpm Qpo1 ¥ 35 ¥

¥ ¥

2 71 ¥ Py

20 ¥ ¥ ¥ fault ¥ Qay ¥ ˇcp ¥

¥ ˇz 40 11 31 Qca f ¥ 17

QHao T L Qpy ¥ 13 ¥ D

l ¥ Qay 35 ˇm Qca 16 Qpm ¥ a

l ¥ 15 Qay U

80 l 2 ¥ 6 ¥ ¥ ¥ Pa 40 l ¥ 20 ¥ Qre l 23 Ps Ps ¥ ˇcp ¥ Qpo L ¥ ¥ ¥ 2 Pa Qpo

Strike and dip of joint or fracture ˇcp Pg Tsla ˇz 27 u 40 2 17 ¥ ˛m 17' 30" ¥ ¥ 29 ¥ ˇz ¥ ¥ ¥ Qpo3 ¥ ¥ ¥ ˛m 15 76 17'30" A Qay 21 ¥ I ¥ U Pg ¥ 40 ¥ ¥ ¥ 17 ¥ ¥ l

¥ D ˇz Pg 30 Pg10 ¥ Qpo1 20 58 15 14 39 Qpm ¥ 1 QHa X Qay ¥ 20 Py ¥ t 23 ¥ 76 ˇm ¥ ¥ ¥ 06 ¥ ˇm ¥ 45 Qay 16 ˇm 12 ˇm ˇcp ¥ Qca ˇm Qpy ˛m ¥ 10 ¥ 45 Ma ¥ A 10 Qay ¥ ¥ RANDE ¥ 11 ¥ QHa ¥ ¥ ¥ 16 Strike and dip of S foliation 30 Ps Pa 36 ¥ 45 46ˇz t 16

1 ¥ Qca ˛s 37 ¥ Qam F ¥ ¥ 19 Qca

Py ¥

Py ¥ ¥ 45 65 Pg ¥ 35 ¥

¥ ¥ s

G ¥ ¥ ¥ Qay 30

O ¥ Qay ul 21

QHa ¥ 20 l ¥ ¥ a

Qay ¥ Qrp ¥ ¥ 7 Ps ¥ 27 Py ¥ ¥ Py

¥ ¥ 40 t l 20 Qrd? ¥

¥ ¥ 15 Ps 53 a ¥ i Qre T ¥ ¥ ˇz ¥ Ys 80 75 ¥ IO 12 25 ¥

QHao I Pa ¥ Pa 22 ˇm c Qpo Py 37 2 ¥ Strike and dip of S foliation ¥ ¥ 45 ¥ 25 Pg¥ la 20 20 ¥ ¥ 46 45 2 AM M ¥ ¥ Pg Py Pa

6 ¥ Qpo 20 ¥ P 47 ¥

AM R I 3 ¥ ¥ 40

QHa Qpy 60 ¥¥ Qay 21 ¥ ¥ 35 52 Pa47 QHa 30 Ma sf

¥ ¥ ¥ Qca 53 QHa L ¥ 12 ¥ Pa Py 41 ¥ ¥ ¥ a 21 72 39 ¥ ¥ 44 ¥ 80

06 OF 16 18 ¥ Qca t 7 ¥

QTob ¥ Qca ¥ ¥ ¥ ¥ 5 ¥ ˛s

¥ ¥ AM N Qay 10 15 ˛m ¥ ¥ ¥ ¥ ¥

Strike and dip of magmatic foliation in granite defined by alignment of megacrysts . (Qay) ¥ ¥ ¥ ¥ ˛s Qca 38

¥ 25 Pa Qss 8 ¥ R 30 11 50 23 ¥ 85

Qam ˛s ¥ er

Qay Qpm l ¥ 26 2 E ¥ ¥ ¥ ¥ 34 10 l ¥

¥ ¥ u AM ¥ ¥ Xms ˛m ˛m Qay IMIT T Ma 27 Qay

56 Pa ¥ Qca 43 17 Qpo2 ¥ ¥ daf Qre S 16 55 ¥ ¥ ¥ 10 Qpo2 ¥ 22 35 50 Qca 10 ¥ ¥ H 37

Magmatic foliation in granite defined by mafic enclaves L ¥ 52 35 Qpo¥ 10 A 2 Qre ¥ Qca 19 ¥ 55 85 10 m 74 RG59356 26 24 QHa E ¥ 10 ¥ s Qpm1 Ma 17 43 80 14

¥ ¥ ˛m ˛s Ma a 10 RG64146 ¥ 60 E af 34 Xms 70 75

¥ 13 32 Ys L 25 Qpm Xms ¥ l 2

Trend and plunge of lineation—defined by elongate minerals or stretched grains ¥ 11 25 40 22 29 56

Qay l 27 38 ˛s 85 ¥ af Qay ¥ Qca 16 7 85 t ˛m ˛s 9 8 s

Qay Qpm1 af ASTERN Qpm ¥ ¥ Ma 6 43 usite 2 50 32 ˛s ˛m 15 a Qca¥ ndal QHa E ¥ 10 34 20 A ¥ Ma Ma 62 87 18 83 D U Metamorphic facies—Showing boundary between diagnostic mineral assemblages . RG64485 ¥ Xms 16 34 E illimanite ¥ 30 Ma 7 74 67 24 85 ˛m S Qre ¥ ˛s 74 Xms Qca ˛s 32 9 ¥ QHa Qpy1 22 Xa 7 80 80 70 21 39 Qam Qay Qre ¥ ¥ Qpy Yp 76 64 43 28 15 70 2 m ˛m 05 RG61539 ¥ 31 Ma 20 ˛m l l 43 7 Metamorphic minerals locality— [1] sillimanite; [2] andalusite; [3] sillimanite and K-feldspar; [4] sillimanite - QTob 80 ¥ Xas 73 10 14 Qpy 80 Xa 2 Xss ¥ ¥ ¥ 56 25 85 Qpo1 ¥ QHa 64 72 60 63 ˛s 65 65 16 andalusite +/- K-feldspar and cordierite; [5] sillimanite - andalusite +/- cordierite; [6] chlorite - muscovite +/- SANDIA Qpy ¥ Qay ¥ 3 85 ¥ 1 RG62203 daf ¥ ¥ 27 Qae ¥ Xss 65 ¥85 Qca biotite; [7] wollastonite; [8] calcite + quartz Qpm2 Qpm2 ¥ Xas 2 44 ˛s ˛m 22 QHa 85 ¥ AM Qrd? Xms Yp Qay ˛m

Qrm ¥ 61 3 ¥ QHa 20

Qam af 48 Yp 30 81 84 76 80 Xa Xss 15 Qre Qay ¥ ¥ ¥ 85 ¥

39 Qpm l ¥ Xas 80 30 l 1 af ¥ ¥

05 ¥ 55 Ys 67 Pa 17 5 Pa ¥ QHa 80 Xss 56 ite Ys ¥

Diatomite marker bed at top of Edith Formation (Qre) ? 44 an Qay ¥ ¥ Xa lim e 17 ¥

QHa Qpo2 ¥ Yp Sil sit QTob 78 alu 12 ¥

Qam PUEBLOQHa ¥ And 19 Qrd? 1 ¥ Paleoflow direction—measured azimuths of imbricated clasts AM ¥ ¥ Ys

Qpm2 ¥ Xms 69 Xas 80 ¥ 44 ¥ Xss 70 4 ¥ l l 8 QTt AM QHa ¥ QTsp ¥ 2 45 70 5 12 Qls ¥ Qpm2 76 87 30 AM 50 Qay QHa Rincon fault Xa 45 Xa Ys ¥ Gravels with affinities to western basin-margin deposits Qrp ¥ 62 ¥ Qay ¥ 75 70 72 4 ¥ Qay 36 3 ¥ ¥ Ma ¥ 60 62 ¥ 65 Qrpr 62 ¥ ¥ 4 A ¥ 1 43 ¥ P QHao Qrp Xa Qls ¥ T. 12 N. ¥ ¥

¥ ¥ 2 Yp 72 Xss 83 14 ¥ o p ¥ Gravels with affinities to ancestral Rio Grande fluvial facies l ¥ 30 ¥ ¥ ¥ ¥ 27

¥ ¥ l Qpm 4 ¥ ˛s ˛m AM 2 a

Qpo2 ¥ m 39 e ¥ QTob ¥ D Xa Xas t 63 85 c 04 ¥ si 86 e Qay 15 h 10

Qpy U lu e ¥ 1 ¥ 40 da it 40 67 Xss 46 12 15 Gravels with affinities to eastern basin-margin deposits An an c e 20 ¥ QTsp 36 Xss e Qpm1 illim 5 42 7 af QTsa ¥ ¥ 74 S 81 Xss 34 r Qrd? ¥ 36 27 80 25 72 r 18 Qay1 63 41 26 o 18 l ¥ ¥ 62 69 11 Approximate extent of buried fluvial terrace risers of the ancestral Rio Grande (post Santa Fe Group)—Hachured Qre l 41 21 ¥ 4 58 70 65 8 Qam Qrm ¥ ¥ 39 ¥ Yp 73

towards fluvial terraces; Lomatas Negras Fm. (single hachured line), Edith Fm. (double hachured line), Los ¥ 2 41 Xas 15 f ¥ 04 QTob E' Yp 1 74 Qay a QTsa QTsp ¥ 20 Xa 10 Duranes Fm. (triple hachured line), and Arenal Fm. (quadruple hachured line) Qam ¥ 75 45 u ¥ QTsp Qpo2 79 72 50 f Tsla?¥ Qay ¥ 31 72 0 a 18 l Qpm2 QHa ¥ 44 51 u t l 4 Yp ˛m Pa l Qpm Yp ˛m l ¥ 2 ¥ 42 40 t Xms Xas 34 Xmig 71 12 9 AM Aeromagnetic anomaly (interpreted from U. S. Geological Survey and Sial Geosciences, Inc., 1998) . ¥ 75 76 5 10 RG64408 RG62037 39 41 45 20 QHa2 af Qpy1 65 76 40 Yp 3 72 59 Ys 35 . ¥ ¥ ¥ 52 3 ˛s 13 12 2 ¥ 85 77 Qca Ma ˛m af 62 5 10 Mine or quarry, adit, shaft Qe ¥ Ys 3 6 14 AM ¥ ¥ 75 S Yp Qam l 44 A Xmig 8 l ¥ i 2 l n l 7 20 i 6 Ys d ¥ Yp m

¥ 48 Qca a

¥ W a lu 71 19 Direction of landslide failure and surface movement A Yp 15 15 2 37 n

s ¥ n it h 35 it 38 39 d Tsla? Qpy ¥ i 38 Qay af 2 ¥ e 03 Yp e t Qrp Qrm ¥af af a 29

e 42 lu

¥ Yp ¥ I 30

I M I 27 I ¥ s Xa it ¥ Basalt bed ic l l QHa Qpm1 ¥ ¥ 37 e a

Xss ¥ QHa af QTsp ¥ 7 ˛m

¥ 7 ¥ 8 ¥

Yp Yp 25 e ¥ ¥ I I Qay Xss ¥ I Yp it

Approximate boundary of tuff ring e

I Yp s 20 ¥ ¥ t ¥ I 7 u i 68 ¥

Qay ¥ l n 1 2 a ¥ Qay ¥ a 2 l ¥ Yp d

1 550 000 l Qpm2 47 n im ¥ Pa

af Qpm2 A ll Ys 19 i 72 42 ¥ B5 Selected locality, Placitas (P), and Bernalillo (B) quadrangles ¥ Xas S

FEET ¥ 2 76 Qca 15 QHa 11 af ¥ ¥ 62 9 Yp 61 70

78 70 20 ¥ 5 Qpm1 ¥ 81 ¥

Qpm2 ¥ 68 14 ¥ EFW Water-supply well, included abbreviation ¥ Yp Yp

af Qre l 66 ¥ l ¥ Yp 80 60 Qrp ¥ ¥ Xms ˛s ¥ af ¥ ESA1 Exploratory or groundwater monitoring well, including abbreviation af ¥ 18 57 ˛m Qpm ¥ 1 ¥ ˛m 51 ¥ ˛s 27 79 Ma 15 43 QHa l ¥ QTsa ¥ SHD2 af Qpm l Xa Exploratory geotechnical boring, including abbreviation 2 ¥ Yp 15 10 Qay QHa ¥ 70 47 72 ˛m 10 Tsla? Tsla? 3902000m N. Qpm2 80 16 ˛m Qam Qay ¥ Qpm2 Xas 72 80 16 af AM Yp 9 Las Huertas geomorphic surface QTsp Qpo 20 45 l ¥ 10 l Qpy2 ˛m QHa 89 56 15 Qpm2 Yp Ys 13 25 Qrpr ¥ Xa Tsla? 15

Del Agua geomorphic surface Qrp AM 56 22 67

3902 Qre 50 72 25 27

Ys ¥ ˛s

¥ ¥ Qay QTsa ¥ QTsp

2 Ys ¥ Qca 6 Qpm2 Qpm2 ¥ Xms Xss Ma ¥ QHa 9

QHa ¥ Ma l Qpo ¥ ¥ Qay l Qpm1 ¥ 26 Tsla? ¥ Ys 35° 15' ¥ 35°15' 3 3 3 3 3 3 3 3 000m 54 56 R. 3 E. R. 4 E. 58 59 60 61 62 364 3 3 3 370 3 3 000m 106° 37' 30" 470 000 FEET ALAMEDA 6.6 MI. 35' ALAMEDA 5 MI. 32' 30" 63 E. 106°30' 430 000 FEET 66 R. 4 E. 67 27'30" R. 5 E. 68 (SANDIA CREST) 25' SAN ANTONITO 14 MI 73 74 E. 106°22'30" ALBUQUERQUE 14 MI. ALBUQUERQUE 12 MI. (ALAMEDA) INTERSTATE 40 20 MI INDEX MAP OF NMBMMR’S (SANDIA PARK) CERRO ARROYO ARROYO WHEELER DE LOS STATEMAP GEOLOGIC QUADRANGLES HONDO SECO PEAK SCALE 1: 24,000 TAOSES MN B' Base from U.S. Geological Survey 1954, photorevised 1972 Base from U.S. Geological Survey 1954 3 GN MN 02/00 36°30' 1 0.5 0 1 MILE TAOS Polyconic projection, 1927 North American datum GN Polyconic projection, 1927 North American datum, 10,000-foot grid based on New OF-DMÐ43 (LOS GRIEGOS) NMBMMR STATEMAP Bernalillo & TRES LOS PUEBLO 10,000-foot grid based on New Mexico coordinate system, cental zone1000-meter Mexico coordinate system, cental zone Quadrangles Placitas OREJAS CORDOVAS PEAK 12.5° Taos Universal Transverse Mercator grid ticks, zone 13, shown in blue 1000 0 1000 2000 3000 4000 5000 6000 7000 FEET ° 1000-meter Universal Transverse Mercator grid ticks, zone 13, shown in blue 0° 54' 13.5 222 MILS ° 01020mi CARSON Dashed land lines indicate approximate locations 0 50' 240 MILS OF-DMÐ22 16 MILS TAOS RANCHOS SHADY West boundaries of San Felipe Grant and Sandia Pueblo Grant adjacient to Rio Grande NEW MEXICO 15 MILS Geologic mapping: S. D. Connell (Quaternary), S. M. Cather (Cenozoic), Bradley Ilg JUNCTION DE TAOS BROOK 1 0.5 0 1 KILOMETER 01020 30km TAOS SW omitted due to insufficient data (S.E. section of quadrangle), C. Andronicus, A. S. Read, and K. E. Karlstrom (Proterozoic), OF-DMÐ12 OF-DMÐ33 B. Menne and M. Picha (M.S. Theses -- Phanerozoic) TRES LYDEN VELARDE TRAMPAS PEÑASCO S. D. Connell: geologic mapping, compilation, Phanerozoic stratigraphy and regional BERNALILLO CONTOUR INTERVAL 10 FEET RITOS UTM GRID AND 1972 MAGNETIC NORTH 285 68 structural interpretation refined from borehole data analyses, unit descriptions and D. J. McCraw, M. M. Mansell, and Glen E. Jones: digital cartographic production GMÐ71 DECLINATION AT CENTER OF SHEET PLACITAS CONTOUR INTERVAL 20 FEET UTM GRID AND 1954 MAGNETIC NORTH 84 correlations, and structural cross sections; geology depicted in areas of disturbance (af LOCATION OF QUADRANGLES DECLINATION AT CENTER OF SHEET SAN JICARITA CHILI JUAN CHIMAYO TRUCHAS EL VALLE PEAK and daf) interpreted from aerial photography PUEBLO NATIONAL GEODETIC VERTICAL DATUM OF 1929 ABIQUIU 1:100,000 TAOS 1:100,000 36°00' D. J. McCraw M. M. Mansell, and G. E. Jones: digital cartographic production RANCHO VALLE PUYE SAN SEVEN VALLE SIERRA TRUCHAS PECOS DEL SAN GUAJE ESPAÑOLA CUNDIYO PABLO SPRINGS TOLEDO MOSCA PEAK FALLS CHAPARRAL ANTONIO MOUNTAIN 84 Mapping of these quadrangles was funded by matching-funds grants from the 1995 and 1997 STATEMAP GMÐ26 GMÐ27 Los SAN Alamos TESUQUE COWLES component of the National Cooperative Geologic Mapping Program coordinated by the LA JEMEZ REDONDO FRIJOLES HORCADO MIGUEL WHITE 285 ASPEN ELK VENTANA SPRINGS PEAK 106° 37' 30" 106°22' 30" MOUNTAIN ROCK RANCH BASIN MOUNTAIN U.S. Geological Survey and the New Mexico Bureau of Mines and Mineral Resources. BLAND GMÐ28 GMÐ34 OF-DMÐ42 GMÐ73 OF-DMÐ47 35° 22' 30" 35° 22' 30" COCHITI HOLY AGUA SANTA FE BEAR DAM OF-DMÐ32 McCLURE HONEY INDEX TO GEOLOGIC MAPPING GHOST GILMAN PONDEROSA CAÑADA MONTOSO FRIA SPRINGS RESERVOIR ROSILLA BOY SPRING PEAK PEAK PEAK RANCH Santa Fe GMÐ33 GMÐ45 OF-DMÐ7 OF-DMÐ31 LOMA SANTO SANTO TETILLA ° ° SAN JEMEZ GLORIETA 106 37'30" ° 106 22'30" OJITO CRESTON DOMINGO DOMINGO PEAK TURQUOISE SETON LOWER 106 30' YSIDRO PUEBLO PECOS ° ° SPRING OF-DMÐ18 OF-DMÐ25 PUEBLO SW PUEBLO HILL VILLAGE COLONIAS 35 22'30" 35 22'30" Canjilon OF-DMÐ26 OF-DMÐ15 OF-DMÐ23 OF-DMÐ11 25 25 OF-DMÐ46 OF-DMÐ14 LOS ALAMOS 1:100,000 OF-DMÐ41 SANTA FE 1:100,000 35°30' Hill SANTA SAN SAN COLLIER MADRID PICTURE DRAW ANA FELIPE FELIPE BULL NORTH 85 CERRO BERNALILLO PUEBLO PUEBLO NE OF-DMÐ40 ROCK GALISTEO CANYON ROWE (SKY VILLAGE NW) CONEJO NW PUEBLO OF-DMÐ49 SAN YSIDRO Connell & Cather OF-DMÐ45 285 (SKY VILLAGE NE) OF-DMÐ19 OF-DMÐ37 OF-DMÐ30 (Cenozoic) ARROYO SAN LOMA DE LAS PLACITAS GOLDEN CAPTAIN FELIPE MACHETE OJO WILDHORSE LAGUNA [1:24,000] CALABACILLAS OF-DMÐ2 HAGAN DAVIS RENCONA Tentative correlations of alluvial units in the study area, based upon stratigraphic relations, MESA HEDIONDA MESA ORTIZ [1:12,000] E Las Huertas Creek (SKY VILLAGE SE) BERNALILLO MOUNTAIN

(SKY VILLAGE) Picha (1982) OF-DMÐ9 OF-DMÐ16 OF-DMÐ50 OF-DMÐ36 OF-DMÐ48 OF-DMÐ39 35°15' COMMENTS TO MAP USERS landscape-topographic position, degree of soil development and physical correlation of units. D a ° e VILLANUEVA 1:100,000 105 30' N r VOLCANO LOS A SANDIA SANDIA SAN KING 44 BENAVIDEZ e A RANCH GRIEGOS u CREST PARK PEDRO DRAW RANCH q r ALAMEDA A geologic map graphically displays information on the distribution, nature, orientation and age relationships of R e Connell u OF-DMÐ10 OF-DMÐ6 OF-DMÐ1 OF-DMÐ29 q G LA MESITA u 40 EDGEWOOD MORIARTY rock and surficial units and the occurrence of structural features. These data are derived from geologic field mapping, b TIJERAS [1:24,000] l OF-DMÐ35 NORTH This Study Connell (1996) Lambert (1968) NEGRA LA MESITA A ALBUQUERQUE SEDILLO NEGRA SE ALBUQUERQUE EAST compilation of published and unpublished work, analyses of borehole geophysics and well-cuttings, and photogeologic WEST OF-DMÐ4 OF-DMÐ20 OF-DMÐ17 OF-DMÐ3 ALBUQUERQUE 1:100,000 35°00' WIND Menne (1989) interpretation. Locations of geologic unit contacts are not surveyed; therefore, the accuracy of contact locations MESA DALIES HUBBELL MOUNT MORIARTY QHa, QHao Q9 Qya ISLETA ESCABOSA CHILILI depends on the scale of mapping and the interpretation of the geologist(s). Portions of the study area were mapped NW SPRING WASHINGTON SOUTH [1:8000] Qrp, Qrp , Qrpr Qfp9 Bernalilloo OF-DMÐ13 OF-DMÐ5 OF-DMÐ8 at scales larger than depicted on the geologic map; therefore, the user should be aware of significant variations in 1-2 Qfa 165 RIO LOS LOS BOSQUE MILBOURN map detail. Any enlargement of this map could cause misunderstanding in the detail of mapping and may result in Qay Q8 TAJIQUE Qya Placitas PUERCO DALIES LUNAS LUNAS PEAK RANCH ESTANCIA SE erroneous interpretations. Site-specific conditions should be verified by detailed surface mapping or subsurface OF-DMÐ21 OF-DMÐ24 Karlstrom, Read, Ilg, Bauer, Qay2 Q7 Qya IO BELEN CAPILLA exploration. NW Johnson, Andronicus R BELEN TOME TOME NEPEAK TORREON EWING MOUNTAINAIR Qrm Qoa2 Qm NE (Proterozoic-Phanerozic) This map has not been reviewed according to New Mexico Bureau of Mines and Mineral Resources standards. OF-DMÐ27 [1:12,000] Qre Qoa1 Qe VEGUITA ° ° Revision of the map is likely because of the on-going nature of work in the region (Please note the date of last MANZANO PUNTA DE 35 15' 35 15' COMANCHE BELEN TURN TOME SE MOUNTAINAIR WILLARD PEAK AGUA ° ° Qpm Q6 RANCH SW 106 37'30" 106 30' 106°22'30" modification in the upper right of Plate I). The contents of this map and associated report should not be considered Qop OF-DMÐ28 BELEN 1:100,000 34°30' Bernalillo Quadrangle – Placitas Quadrangle – final and complete until reviewed and published by the New Mexico Bureau of Mines and Mineral Resources. The 106°00' Qpo Q5, Q4, Q3 LA JOYA SOCORRO 1:100,000 109° 107° 105° 103° Qop BLACK BECKER NMBMMR OF-DM-16 NMBMMR OF-DM-2 NW ABEYTAS 37° views and conclusions contained in this document are those of the authors and should not be interpreted as necessarily BUTTE LADRON Taos QTob, QTsp Q2, QT1 Qu(?)s, Tm SCHOLLE 34° (Connell, 1998) (Connell, et al., 1995) 22' representing the official policies, either or expressed or implied, of the State of New Mexico or the U.S. Government. 30" LA JOYA BECKER Grants SANTA FE SILVER SAN SW CERRO RAYO HILLS CREEK ACACIA MONTOSO 35° Albuquerque Socorro Connell (1998) 106°30' Karlstrom, et al. (1995-9) SAN MESA SIERRA 25 S A N D I A LORENZO LEMITAR DEL DE LA SPRING YESO CRUZ 33° OF-DMÐ38 Deming Las Connell & Cather (1995-8) Menne (1989) Cruces M O U N T A I N S LOMA WATER BUSTOS SOCORRO DE LAS ° ° CANYON WELL 35 15' 35 15' CANAS Picha (1982) OF-DMÐ34 Location Map 106° 37' 30" 106°22' 30" 107°00' Physiography of the Bernalillo - Placitas area based upon 10-m USGS DEM data. NMBMMR Open File Map Series OF–GM–2 and OF–GM–16 NEW MEXICO BUREAU OF MINES AND MINERAL RESOURCES PLATE II of III. A DIVISION OF NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY

ines & Mine f M ra o l R MEX u e I a s W C A' e o East r u E O u r B c N E e Placitas M s

N New Mexico Tech Las Huertas S fault 16,000 E T P ar ry fault feet ASL th ntu A A Scie t Ce T nce for the 21s E M West Dr. Paul W. Bauer 15,000' Dr. Peter A. Scholle Geologic Mapping Las Huertas Director and State Geologist Kmf Program Director fault 14,000' Caballo Kmu Khd 13,000' Kmf fault Kmf Kmu Kml Geology of the Bernalillo and Placitas Khd Kd 12,000'

quadrangles, Sandoval County, Kml Kmu Jm Khd A Kd Jt 11,000' Je New Mexico NW Valley View Ranchos Jm Kml Kd Bernalillo faults Jt 10,000 Jt ˇcp 10,000'

Ranchito LACITAS feet ASL Luce ult Jm Kmf Je

ERNALILLO fa P fault Je ˇz B Tsp 9,000' fault Km c ˇcp 9,000' PLATE II of III. fault u Kmf ˇcp ˇm RIO RANCHO/ Khd fault fault Km ˇz Py u Pg fault ˇm ˇcp Ps ˇz Khd 8,000' PUEBLO OF PLACITAS Ps 8,000' GEOLOGIC CROSS SECTIONS Kml Kmf Pg ˇm ˇm Pa Pg ˇz Kmf Km Py Tspc u Ps SANTA ANA Khd Ps BERNALILLO Kd Kml ˛m 7,000' Py 7,000' 1:24,000 Tspc Kmu Jm Xu Rio Kmf ˛s Khd Pa Jt Kd Kml ˛m ˛s Kmu Km Kmf Pa Pa u Kd Khd Kmf Kml Je Jt Jm Khd ˇcp Jm Ma 6,000' Km Ma ˛s ˛m 6,000' Grande Kml l Pa Pa Qpm Kmu Kml Je Jm 17 February 2000 Revision Qae/Qam Khd Jm Qae/Qay QHa Kd ˛m Qre Kd ˇcp Jt Qrp QTspcs Kml Je 5,000' Jm ˛m 5,000' Jm Kd Jt Je ˛s ˇz ˇm QTo Jt Jm Ma Je ˛m Xu ˇcp ˇcp ˛s Jt Pg Ps QTsa QTspcs Kmf Je Py ˛s Ma 4,000' QTo Jt Pg 4,000' Je ˇm Bernalillo quadrangle QTo ˇcp ˇm Je ˇz ˇz Kmu Khd Pa Xu Xu NMBMMR OF-DM-16 QTo Ps Tg? Pg Ma 3,000' ˇcp ˇz 3,000' ˇm Py Py May 1998 Kml ˇz Ps ˇm Pg Ps Kd ˇz Py ˛m Pa 2,000' Jm Py Pg 2,000' Sean D. Connell1 Tz Kmf Ps Pa ? Pg ˇm Pa ˛s Ma Xu 1,000' Tz 1,000' Kmu Pa Xu Tsp Khd ˛m Xu ˛s ˛m Ma Placitas quadrangle ˛s 0 SL Kml 0 SL Tz ˛s DRINKING WATER AQUIFERS Ma NMBMMR OF-DM-2 ˛s Kd Xu June 1995 Tg ˛s -1,000' Tz Jm Ma -1,000' Jt

1 2 3 Te? Je Pa Xu Sean D. Connell , Steve M. Cather , Bradley Ilg , -2,000' -2,000' 3 3 3 Kmf Tg ˇcp Karl E. Karlstrom , Barbara Menne , Mark Picha , ˛m Tg 3 2 2 Xu Chris Andronicus , Adam S. Read , Paul W. Bauer , -3,000' ˛s Ys -3,000' ˇm ˇz Ma 2 Kmu Khd and Peggy S. Johnson Tg Kmf Pg Ps -4,000' Py -4,000' Kml Kmf 1New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801, Kd

Albuquerque Office, Albuquerque, NM 87106 Kmu Pa Khd 2 -5,000' -5,000' New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801 Kmu Kmf Jm Khd 3Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131 Jt Ys Kml ˛m -6,000' Je ? -6,000' Kml Kmu Khd Jt Kd Jm ˛s ˇcp Kd Je Ma -7,000' -7,000' Kml ˇz Jm ˇm Psg ˇcp Ys Jt ? -8,000' Kd -8,000' Je Jm Xu ˇz Jt Pay ˇcp Psg Xu -9,000' -9,000' Je ˇm Pay ˇz ˇcp ˛m ˇm Pay Psg ˛m -10,000' -10,000'

Placitas fault zone B' B S CROSS SECTION LOCATIONS N 16,000 106°37'30" B 106°22'30" 16,000 Placitas feet ASL 35°22'30" 35°22'30" feet ASL Kmf fault Km u Khd 15,000' 15,000' Kml Kd D A C' Jm 14,000' C Cross sections are constructed based upon the interpretation of the authors made 14,000' Jt from geologic mapping, and available geophysical (regional gravity and aeromagnetic Je surveys), and subsurface (drillhole) data. Cross sections should be used as an aid D' Bend in 13,000' to understanding the general geologic framework of the map area, and not be the 13,000' ˇcp Cross Section B-B' A' sole source of information for use in locating or designing wells, buildings, roads, Kmf or other man-made structures. ˇm ˇz 12,000' 12,000' Ps Pg Py E Kmu 11,000' E' 11,000' Khd Pa Kmu 35°15' 35°15' Khd Kml 10,000' 106°37'30" 106°30' B' 106°22'30" 10,000' Kml Kmf Kd Bernalillo Quadrangle – Placitas Quadrangle –

Kmu ˛m NMBMMR OF-DM-16 NMBMMR OF-DM-2 PLACITAS Khd 9,000' (Connell, 1998) (Connell, et al., 1995) 9,000' Jm ˛s Ma Jt Je Ys Kml 8,000' 8,000' Kmf Lomos Kd Xa Xss ? Jm ˇcp ? Km Xas 7,000' 7,000' u Jt ˛s Xa Xa D D' fault Khd Je ˇm Las Huertas Kd WNW Jm ˇcp ˇz ESE geomorphic surface Kml Jt Xss 6,000' 6,000' Ys 5,600 5600 Qss Qss Qss Py feet ASL feet ASL QTst Tsp Xas Ancestral Rio Grande terraces Qre and Qpm Qpm c ˇcp Qrp and QHa Xa 5,000' 5,000' QTsa Xms ˇz QTsa QTo QTsa Te ˇm ˛m Pg Ps 4,000' 4,000' Tg 5,400' Inner valley of the Rio Grande 5400'

Py ) QTst Kmf Xas Xa QTo QTspcs ˛s 3,000' 3,000' QTspcs Ma Qam Projected base of Qrl

Pa ( projected RWP-14 ? Xa SASF1 Te Qpm Khd ) QTsp Kmu Xa 2,000' 2,000' cs 5,200' 5200' Tg QTo Qre Qre

Xms SAP1 Kml

Qay Rio Grande RG51722 ( projected SAP2 1,000' ? SHD-B1 1,000' Tsp c QHa Kd Qam Qrd? SHD2 Je ˛m Ma SHD1 Jm Xa Xas Qrp ? ? 0 SL ? ? 0 SL Jt 5,000' TD 5000' 43 ft QTsa TD TD 265 ft 118 ft Km TD u 101 ft ˇcp ˛s -1,000' QTo QTo ? -1,000' Khd ˇm TD 180 ft Kmu ˇz Ys

Xas TD TD TD Vertical Exaggeration =10x 810 ft -2,000' 800 ft

Ps 1,043 ft -2,000' 4,800' 4800' Pg Py

Ma Pa Xms Xa Xss -3,000' -3,000'

Xas No Vertical Exaggeration ˛m ˛s -4,000' -4,000'

San E E' Francisco WNW ESE fault 5,800 5800 feet ASL feet ASL

Ancestral Rio Grande terraces Escala Las Huertas fault geomorphic surface

East Ps C' 5,600' 5600' C West Valley View Escala Pg E W Valley View syncline Py Inner valley of the Rio Grande fault ? 7,000 fault ˇm 7,000' feet ASL Pa ? Ps Bend in Qay Pg 6,000' EFW 6,000' 5,400' ? 5400'

BRE Qay Cross Section E-E' Py ? RG4980252 ˛m Pa 5,000' TD TD 5,000' 610 ft 495 ft Tsp c Projected base of Qrl TD ˛s ? QTsa 700 ft QTsa Qpm ? QTspcs 4,000' ˛m 4,000' 5,200' ) 5200' Qam RG-64146 Qrm Horizontal Scale QTsp Ma ? ? Qre 1 0.5 0 1 Mile Qam-Qrd ? 3,000' 3,000' ? Te QTsa RG-62037 ( projected Tsp s? Qay QTst ˛s 1000 0 1000 2000 3000 4000 5000 6000 7000 Feet Qrd? ? Y/Xu 2,000' 5,000' Qrp 2,000' Tg ? 5000'

Y/Xu ? QTo 1,000' Tsp c? 1,000' QTo Kmu Kmf TD 170 ft ? Khd Km No Vertical Exaggeration TD l 335 ft ? Vertical Exaggeration =10x 0 SL 0 SL 4,800' 4800' NEW MEXICO BUREAU OF MINES AND MINERAL RESOURCES NMBMMR Open File Map Series A DIVISION OF NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY OF–GM–2 and OF–GM–16 PLATE III of III. Alluvium Middle and lower Santa Fe Group, undivided Mississippian ines & Mine Eastern-basin margin piedmont deposits f M ra Divided into stream-valley alluvium, western-margin alluvium, and eastern-margin piedmont alluvium. Stream-valley alluvium (QHa and o l R MEX u e a s IC Qay units) typically contain poorly to well sorted, poorly to well stratified, clast- and matrix-supported deposits associated with modern Piedmont deposits, undivided (lower Pliocene(?) to Miocene) — Cross section only. Slightly to moderately tilted, well consolidated, Arroyo Peñasco Group, Espiritu Santo Formation, undivided (locally includes the Log Springs Formation) — These are the e o W Tsp Ma r u E O and late Pleistocene entrenched arroyos across the map area. Gravel composition reflects upland lithology. Stream-terrace deposits and well cemented, sandstone and limestone-dominated conglomerate, sandstone, and mudstone derived from the Sandia Mountains oldest sedimentary rocks in the area and rest unconformably on a relatively planar surface of Proterozoic basement. The Espiritu Santo u r B c N typically have an elongate planform shape and are associated with major drainages. Western-margin alluvium is delineated west of and eastern-basin margin. Deposits are generally better cemented and more steeply dipping than overlying upper Santa Fe Group Formation is composed of a basal member, the Del Padre Sandstone, and an unnamed upper member. Mississippian exposures are e M s the inner valley of the Rio Grande (Qam and Qao units) and generally contains poorly to moderately sorted, moderately stratified, and eastern basin-margin piedmont deposits (QTsp, QTspc, QTspcs, QTsps, and QTspsm). May be correlative to piedmont-slope and alluvial discontinuous with the thickest section in the vicinity of the Sandia Mountains found on the west slope of the Crest of Montezuma N New Mexico Tech clast and matrix supported deposits derived from uplands underlain by deposits of the Arroyo Ojito Formation (Loma Barbon and Ceja(?) fan deposits of the Sierra Ladrones or Popotosa formations (Machette, 1978) exposed at the southern margin of the Albuquerque Basin. (generally only the basal Del Padre Sandstone is recognized). The Del Padre Sandstone, about 6 ft (2 m) thick, is a distinctive quartz- cobble conglomerate overlain by a very coarse-grained, green and purplish-brown sandstone. Stromatalitic limestones, about 30 ft (10 S Members). Eastern-margin piedmont alluvium (Qpo and Qpm units) contains generally poorly sorted, poorly stratified, clast- and matrix- Estimated thickness is approximately 9,840 ft (3,000 m). Locally divided into five mappable subunits based on dominant deposit texture supported deposits having angular to subangular clasts of granitic, metamorphic, sandstone, and minor limestone derived from the m) thick, are above the basal Del Padre Sandstone followed by limey mudstones, dolomites and minor wackestones. Microfossils found E T P (see Cather, 1997) and clast composition. a ry rth tu A western and northern slopes of the Sandia Mountains and eastern basin margin. above the Del Padre Sandstone member indicate an Osagean age (Armstrong and Mamet, 1974). Undulose extinction and sutured Sci Cen A ence for the 21st T E M Piedmont deposits, limestone-bearing conglomerate subunit — Well consolidated and cemented, limestone-dominated gravel quartz grain boundaries in thin sections of the basal conglomerate suggest a pre-Pennsylvanian tectonic history (Read et al., 1999). Tspuc Unconformably overlying the Espiritu Santo Formation, on the west slope of the Crest of Montezuma, are fluvial red shales and siltstones Stream-valley alluvium capping the top of Lomos Altos. Recognized by an abrupt increase in limestone clasts. Approximately 40 ft (12 m) thick. Dr. Paul W. Bauer of the Log Springs Formation (6 - 10 ft or 2 - 3 m thick) that are not differentiated from the Arroyo Peñasco Group. The total measured Dr. Peter A. Scholle Piedmont deposits, conglomerate subunit — Conglomerate (conglomerate:sandstone ratio of 2) with subordinate sandstone. thickness of the Arroyo Peñasco Group is 73 ft (22 m) on the west slope of the Crest of Montezuma (Armstrong and Mamet, 1974). Youngest stream alluvium (Historic to Holocene) — Unconsolidated deposits of brown, light gray-brown, and yellowish-brown (10YR) Tsp c Geologic Mapping QHa sand, silty to clayey sand, and gravel. Boulders are common along the base of Rincon Ridge and northwestern front of the Sandia Mudstone is absent. Conglomerate is mostly clast supported, although matrix-supported deposits are locally present. Clast content Director and State Geologist varies upsection. Phaneritic early Tertiary volcanic clasts derived from the Espinaso Formation (Te) are present near the base of Program Director QHao Mountains. Inset against eastern-margin piedmont alluvium (Qpm2) and stream alluvium (Qay). Underlies modern arroyos that grade westward to the Las Padillas Formation (Qrp, Rio Grande floodplain). Very weakly developed soils exhibit no pedogenic carbonate at the section exposed along the southern end of the Cuchilla de Escala (Locality P7), with Paleozoic and Proterozoic detritus PROTEROZOIC ERATHEM the surface and weak Stage I carbonate morphology at depth. Locally subdivided into an older (QHao) deposit on the basis of inset dominating upsection. Volcanic pebbles and cobbles are absent at Lomos Altos (Locality P8). relationships. Forms extensive valley border alluvial fans along the margins of the inner valley of the Rio Grande. These valley border Mesoproterozoic alluvial fans may locally contain hydrocollapsible soils. Geomorphic surface Q9 of Connell (1995, 1996). Variable thickness, up to Piedmont deposits, conglomerate and sandstone subunit — Subequal sandstone and conglomerate. Mudstone is rare. Tsp cs Sandstone is medium- to very coarse-grained and is typically horizontally laminated or trough crossbedded. Conglomerate is mostly Pegmatite and aplite dikes — Dikes, pods, and lenses ranging from <1 in. up to >50 ft (<3 cm to >15 m) in thickness and up to 1 mi. 40 ft (12 m). Yp clast supported and consists largely of Paleozoic limestone, sandstone, siltstone, and chert with subordinate Proterozoic lithologies. (1.6 km) in length; interpreted to be coeval with the Sandia granite (Ys).

Qay Younger stream alluvium (Holocene to uppermost Pleistocene) — Poorly consolidated deposits of very pale-brown to light-brown Geology of the Bernalillo and Placitas (7.5-10YR) sand to sandy clay loam and gravel. Inset against alluvium of units Qpm and Qam. Slightly dissected surface possesses Piedmont deposits, sandstone subunit — Sandstone (conglomerate:sandstone ratio is less than 0.5), with subordinate siltstone. Ys Sandia granite — Mainly megacrystic biotite monzogranite to granodiorite. K-feldspar megacrysts, up to ~1 in. (3 cm) long, are Tsp s Sandstone is mostly horizontally laminated with subordinate trough and planar crossbedding. Conglomerate occurs in shallow, commonly aligned in a magmatic foliation. Contains numerous ellipsoidal enclaves of microdiorite, fine-grained granite, and gabbro Qay2 well-developed constructional bar-and-swale topography. Weakly developed soils exhibit Stage II carbonate morphology and minor clay film development. Associated with broad valley fill units within modern stream valleys that grade to the Las Padillas Formation (Qrp, lenticular beds, is mostly clast supported, and consists dominantly of pebbles of Paleozoic sedimentary rocks and lesser amounts (interpreted to be mingled mafic magmas), and xenoliths of quartzite and mafic metavolcanic rock. Pegmatite and aplite dikes ( Yp), quadrangles, Sandoval County, Qay of Proterozoic crystalline rocks. Siltstone is massive to faintly laminated and forms tabular to broadly lenticular beds. and quartz veins are ubiquitous. Various radioisotopic dates are available: U-Pb-zircon+sphene yields an age of 1,455±12 Ma (Tilton 1 Rio Grande floodplain). Hibben (1941) reported Rancholabrean mammals (Mastodon and Equus) within this unit near the Village of ± Placitas (see also Kelley and Northrop, 1975, p. 72-73). Archaic (2-6 ka) projectile points were also reported in this deposit (probably and Grunenfelder, 1968, recalculated by S. Getty, unpublished); U-Pb-zircon yields an age of 1,437 47 Ma (Steiger and Wasserburg, Tsp Piedmont deposits, siltstone and mudstone subunit — Subequal siltstone and mudstone, with rare sandstone. . 1966, recalculated in Kirby et al., 1995); U-Pb-zircon yields an age of 1,446±26 Ma (Unruh, unpublished data); 40Ar/39Ar data yield near the deposit base) just north of state highway NM 165, near the Village of Placitas (Bruce Huckle, UNM Maxwell Museum, 1999 sm ± ± New Mexico written communication). Locally includes undivided stream alluvium (QHa) in narrow arroyos. Locally divided into older (Qay ) and an age of 1,422 3 Ma from hornblende and 1,423 2 Ma from muscovite (Kirby et al., 1995); apatite fission track dates range from 1 14 ±4 Ma at low elevation to 30±5 Ma at high elevation (Kelley et al., 1992). younger (Qay2) subunits on the basis of inset relationships at the southwestern corner of the Bernalillo quadrangle. Spring deposits are locally interbedded within reaches of the Arroyo de San Francisco (notably in Section 15, T13N, R5E). Forms broad valley border alluvial fans along the margins of the inner valley of the Rio Grande. These valley border alluvial fans may locally contain hydrocollapsible Volcanic and intrusive rocks soils. Geomorphic surface Q8 of Connell (1995, 1996). Variable thickness, up to 70 ft (21 m). Paleoproterozoic Tvc Canjilon Tuff (upper Pliocene) — Oval-shaped tuff-breccia diatreme that intrudes east-tilted sandstone of the Loma Barbon Member CORRELATION OF UNITS PLATE III of III. (QTob), just south of Santa Ana Mesa. Generally dips 50° or less towards the center of the diatreme; bedding is subvertical near faults. Western-margin alluvium Contains numerous basalt dikes and brecciated basalt dikes, flows and plugs, where mappable, that are differentiated as basalt and basaltic breccia beds of the Canjilon Tuff (Tvcb). Contains a circular tuff ring near the center of diatreme. Map of diatreme interior is Y/Xu Meso/Paleoproterozoic rocks, undivided — Cross section only. SEDIMENTARY IGNEOUS Middle western-margin alluvium, undivided (upper to middle Pleistocene) — Poorly consolidated deposits of yellowish-brown simplified from Kelley and Kudo (1978). Qam Xr Metarhyolite — Multiply deformed, fine-grained, quartz-muscovite schist with distinctive fine-grained quartz porphryoclasts (eyes) MAP UNIT DESCRIPTIONS AND to reddish-yellow (7.5-10YR) sand to silty-clayey sand and minor gravel. Gravel is primarily composed of red granite, chert, basalt, and (interpreted to be relict quartz phenocrysts). These rocks are exposed in the core of the Crest of Montezuma monocline beneath the Polarity

Basalt and basaltic breccia beds — Locally brecciated basalt flows and feeder dikes interlayered within the Canjilon Tuff (Tvc). Isotope Stage

minor gray volcanic rocks recycled from the Arroyo Ojito Formation. Locally well stratified and slightly cemented with calcium carbonate. Tvcb Epoch Chron Marine Oxygen Yields a K-Ar date of 2.61±0.09 Ma (Kudo et al., 1977) and 40Ar/39 Ar dates of 2.14±0.66 Ma and 2.52±0.43 Ma (Locality Arroyo Peñasco Group (Ma) and bounded by the East Las Huertas fault to the west. 0 ka Inset against older western-margin alluvium (Qao) and is inset by young stream alluvium (Qay). Soil development is variable and Qrpr B-2 and B-3; NMGRL 9132 and 9131, respectively, W.C. McIntosh, 1998, written communication). . Qrpj QHa af daf Qe possesses Stage II to III carbonate morphology. Delineated west of the Rio Grande, where deposits are associated with broad valley Holocene North American QHao Amphibolite and amphibole-biotite schist — Massive green amphibole-plagioclase schist with lensoidal bodies of calc-silicate and 1 Qrp2 CORRELATION OF UNITS Xa Land Mammal "Age" Qrp fill units that interfinger with the Los Duranes Formation (Qrd). Correlative to eastern-margin piedmont alluvium (Qpm) and geomorphic Qrp1 calc-pelite interlayered with amphibolite and metapelite. Protolith is interpreted to be volcanic. 10 2 Qae surfaces Q6-Q7 of Connell (1995, 1996). Variable thickness, up to 200 ft (61 m). Tbsa Basalt of Santa Ana Mesa (upper Pliocene) — Tholeiitic flood basalt with modal affinities to alkali olivine basalt (Kelley and Kudo,

2 Qca

1978, p. 9). Locally, a thin (0-13 ft or 0-4 m thick), discontinuous basaltic tuff locally underlies the base (Spiegel, 1961, Cather and Qay

Xms Qay

± Mica schist and phyllite — Quartz-muscovite schist and phyllite with local andalusite porphyroblasts, commonly crenulated. . Qpy Older western-margin alluvium, undivided (middle to lower Pleistocene) — Poorly consolidated deposits of light reddish-brown Connell, 1998). Bachman and Mehnert (1978) report a K-Ar date of 2.5 0.3 Ma. In the adjoining San Felipe quadrangle, Cather 1:24,000 Qao 40 39 ± ± 1 (7.5-10YR) sand with pebble to cobble gravel interbeds primarily composed of red granite, chert and basalt recycled from the Arroyo and Connell (1998) report Ar/ Ar dates of 2.24 0.22 to 1.77 0.21 Ma (NMGRL 8926, 8927, 8928) for this unit. Variable 3 1

Xas Andalusite-biotite schist — Pelitic andalusite and biotite schist, locally contains chlorite. Qay Ojito Formation. Unconformably overlies upper Santa Fe Group deposits (QTob, QToc(?)), and the Lomatas Negras Formation (Qrl). thickness between 20-40 ft (6-12 m) along southern margin of Santa Ana Mesa. Qpy

Qra Qpy

late Qls Inset by western-margin alluvium (Qam). Unit is poorly exposed and commonly capped by thin veneer of undivided eolian and alluvium Xss Sillimanite-biotite schist and gneiss — Pelitic sillimanite and biotite schist and gneiss, locally contains K-feldspar. . (Qae). Soil development is variable and possesses Stage I to III carbonate morphology. Delineated west of the Rio Grande, where Tmi Mafic or intermediate dike (upper Oligocene) — A single, approximately 4,000 ft (1,250 m) long, northeast-trending mafic to Major unconformity intermediate dike, about 0.6 mi (1 km) north of the village of Placitas (San Antonio de las Huertas Grant). Unconformably overlain by deposits are associated with broad valley fill units overlie the Lomatas Negras Formation. Generally correlative to older eastern-margin 2b Santa Fe Group eastern basin-margin piedmont deposits (Tspc) and yields a 40Ar/39 Ar date of 30.9±0.5 Ma (NMGRL 3183, W. C. piedmont alluvium (Qpo) and geomorphic surfaces Q3-Q5 of Connell (1995, 1996). Variable thickness, up to 50 ft (15 m). 5 2 Qpm

McIntosh, 1995, written communication). Qrm Qpm 128 2a Qcb 17 February 2000 Revision Qrd Qpm

Eastern-margin piedmont alluvium Qpm Paleogene System Younger eastern-margin piedmont alluvium (Holocene to uppermost Pleistocene) — Unconsolidated deposits of brown, light Qpy gray-brown, and yellowish-brown (10YR) sand, sandy clay loam and gravel. Boulders are common along mountain-front alluvial fans 7 Te Espinaso Formation (Oligocene) — Cross section only. Unit comprises the remnants of widespread, coarse-grained, volcaniclastic Brunhes

along the flanks of Rincon Ridge and northern Sandia Mountains. Deposit surface is weakly dissected and possesses well developed Rancholabrean Qpy aprons that accumulated adjacent to volcanic vent complexes of the Ortiz Mountains. Consists primarily of upward-coarsening or crudely Bernalillo quadrangle 2 bar-and-swale topography. Soils possess Stage I to II+ carbonate morphology and few thin clay films. Locally subdivided into older stratified tuffaceous sandstone, conglomerate, and debris-flow deposits. Variable thickness, up to 4,265 ft (1,300 m). . 9 Qpm1 Qpy1 (Qpy1) and younger (Qpy2) subunits on the basis of soil-profile and inset relations. Commonly buries the Edith Formation (Qre) and Qre NMBMMR OF-DM-16 terminates against the escarpment of the inner valley of the Rio Grande. Geomorphic surface Q9 of Connell (1995, 1996) Variable Tg Diamond Tail and Galisteo Formations, undivided (Oligocene to upper Paleocene) — Cross section only. Unit consists of red to Qam thickness, up to 120 ft (36 m). white mudstone, sandstone, and conglomerate deposited within fluvial channels and broad floodplains in an early Tertiary basin between 11

May 1998 Albuquerque and Santa Fe, New Mexico. Previous workers (Stearns, 1953; Kelley and Northrop, 1975; and Menne, 1989) have middle Middle eastern-margin piedmont alluvium, undivided (upper to middle Pleistocene) — Poorly consolidated deposits of very pale- mapped Galisteo Formation in the area (NE1/4 of Section 36, T13N, R4E); however, relatively poor exposures, faulting, and ambiguous 13 Major unconformity Qpm brown to light-brown (7.5-10YR) sand to silty and clayey sand, and gravel derived from the Sandia Mountains. Unconformably overlies textural and stratigraphic relationships preclude differentiation on the map. Variable thickness, up to 4,250 ft (1,295 m). Pleistocene the Edith Formation (Qre) and is inset by younger stream alluvium (Qay). Gravel clasts are predominantly subangular metamorphic and 15 Qpo4 1 Qrl Sean D. Connell porphyritic granite along the western mountain front, and dominated by limestone and sandstone with subordinate granite and metamorphic Qpo rocks along the northern flank of the Sandia Mountains. Granite and limestone clasts are moderately to deeply pitted, and schist clasts MESOZOIC ERATHEM Qpo3 are locally slightly split. The slightly dissected deposit surface possesses subdued, constructional bar-and-swale topography on interfluves. 19 Weakly developed soils exhibit Stage II to III+ carbonate morphology and minor to moderate clay film development. Locally divided Upper Cretaceous Qpo2 into two subunits. Variable thickness, up to 140 ft (43 m). 780 21 QTt

Qao Qpo1 Placitas quadrangle Middle eastern-margin piedmont alluvium, younger subunit (upper to middle Pleistocene) — Moderately consolidated not Qpm2 Kmf Menefee Formation, undivided — Contains three informal members: a lower member (324 ft or 99 m thick), the Harmon Sandstone Major unconformity deposits of very pale-brown to strong yellowish-brown (7.5-10YR), poorly to moderately stratified and sorted, silty clay and loamy (140 ft or 43 m thick), and an upper member (740 ft or 225 m thick). Upper and lower members are similar and contain, in order of shown NMBMMR OF-DM-2 Qpm2a sand and gravel. Inset against eastern-margin piedmont alluvium (Qpo and Qpm1), and conformably overlies the Menaul Formation abundance: gray, tan to orange-tan, cross-bedded, and laminated to thick-bedded siltstone and sandstone; dark-gray to olive-gray and (Qrm). Deposit surface along the mountain front is slightly to moderately dissected and exhibits subdued bar and swale topography Irvingtonian ?? Qss Qpm2b black shale; dull, dark-brown to shiny black lignitic coal; and maroon to dark-brown iron concretions. The upper member has a greater June 1995 on interfluves. The top of the deposit is deeply dissected along the eastern escarpment of the inner valley of the Rio Grande. Soils abundance of shale, carbonaceous material, ironstone, thicker coal seams, and lenticular beds of calcareous sandstone. The light-gray early Local unconformity are moderately developed and possess Stage II carbonate morphology and few to common, thin to moderately thick clay films. to buff or gray-tan Harmon Sandstone is a medium grained, well-sorted, quartz sand with cross-bedding and limonite staining. Thickness Locally divided into older (Qpm2a) and younger (Qpm2b) deposits on the basis of inset relationships. Remnants of a broad, west- of the Harmon Sandstone is variable and thins to at least 73 ft (22 m) in the Hagan embayment east of Placitas. The lower contact s sm sloping constructional piedmont-slope, herein named the Del Agua geomorphic surface, are preserved on the younger subunit between the Menefee Formation and the Point Lookout Sandstone (Kpl) is interfingering and gradational. Total unit thickness varies Matuyama c (locally mapped as Qpm2b) between Del Agua Cañon and Sandia Wash. Geomorphic surface Q7 of Connell (1995, 1996). 1.8 Ma cs 1 2 3 regionally from 680 ft to 1,200 ft (205 m to 365 m) due in part to post-depositional erosion. CENOZOIC

QTsp Tsla Sean D. Connell , Steve M. Cather , Bradley Ilg , QTsp QTsp Middle eastern-margin piedmont alluvium, older subunit (middle Pleistocene) — Moderately consolidated deposits of light- QTst QTsp 3 3 3 Qpm1 Kpl Point Lookout Sandstone — Gray-tan to light-tan and drab-yellow, very fine- to fine-grained, massive, quartz sandstone with limonitic Neogene & Quaternary) (Tertiary Karl E. Karlstrom , Barbara Menne , Mark Picha , to strong-brown (7.5YR) and very pale-brown to light-gray (7.5-10YR), poorly to moderately stratified and sorted, sand clayey sand sandstone lenses and interbedded thin gray shale. The unit is weakly cemented and a prominent ridge- and ledge-former. Both upper Tbsa 3 2 2 and gravel. Inset against older eastern-margin piedmont alluvium (Qpo) and unconformably overlies the Edith Formation (Qre). and lower contacts are interfingering and gradational. Unit thickness ranges from about 240 ft (73 m) near Placitas, to 315 ft (96 m) Chris Andronicus , Adam S. Read , Paul W. Bauer , Dissected deposit surface exhibits subdued erosional ridge-and-ravine topography. Subdued bar-and-swale constructional topography Tvc Tvcb in the Hagan embayment. QTo QToc? QTsa late 2 is locally preserved on broad non-dissected interfluves. Moderately well developed soils with Stage III+ carbonate morphology Tspuc and Peggy S. Johnson and many moderately thick clay films. Geomorphic surface Q6 of Connell (1995, 1996). Mancos Shale, upper member — Medium- to dark-gray to olive-gray shale, and silty shale, with less abundant very fine to fine-

Kmu Gauss grained, locally gypsiferous sandstone. This unit is an upper tongue of the lower member of the Mancos Shale (Kml) and forms valleys Blancan QTob Qpo Older eastern-margin piedmont alluvium (middle to lower Pleistocene) — Poorly to moderately sorted and stratified gravel and and covered slopes between the more resistant Point Lookout Sandstone (Kpl) and Hosta-Dalton Sandstone (Khd). The unit produces sand with minor silty-clay mixtures. Granite clasts are commonly grussified or deeply pitted, schist clasts are typically split, and limestone 1 poor quality, high sulfate ground water. Upper and lower contacts are gradational. Thickness is variable and difficult to measure due ??

New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801, Pliocene clasts are moderately to deeply pitted. Map relationships suggest that deposits are inset against the gravel of Lomos Altos (Tsla) and to cover but ranges from about 240 ft (73 m) west of Placitas, to 360 ft (110 m) in the Hagan embayment. . Albuquerque Office, Albuquerque, NM 87106 are truncated by a buried escarpment formed during deposition of the Edith Formation. Locally divided into four subunits. Variable thickness, ranging up to 46 ft (14 m). Tobc 2New Mexico Bureau of Mines and Mineral Resources, Socorro, NM 87801 Khd Hosta-Dalton Sandstone — Drab, yellow-gray to yellow-tan, very fine- to medium-grained, weakly cemented sandstone with olive-

brown sandstone lenses. The unit is a moderate ridge- and ledge-former. Upper and lower contacts are gradational. Unit thickness ranges early 3Department of Earth and Planetary Sciences, University of New Mexico, Albuquerque, NM 87131 Gilbert c s

Older eastern-margin piedmont alluvium, youngest subunit (middle Pleistocene) — Poorly exposed cobble gravel overlying cs from 210 ft (64 m) near Placitas to 370 ft (112 m) in the Hagan embayment (where it contains a considerable amount of siltstone and sm Qpo4 a strath along the southern margin of Las Huertas Creek. Inset against older eastern-margin piedmont deposits (Qpo3). Deposit is fissile shale that does not exist in the Placitas area). 5.3 Tsp Tsp Tsp inset by the Edith Formation (Qre). Approximate thickness is less than 10 ft (3 m). Tsp Mancos Shale, lower member — Lithology is similar to the upper Mancos Shale (Kmu) with subequal proportions of olive-brown to ? ? Older eastern-margin piedmont alluvium, younger subunit (middle Pleistocene) — Moderately consolidated deposits of Kml not shown Qpo3 gray to black shale and laminated to interbedded, olive-brown to gray, very fine grained sandstone, siltstone, and shale. Selenite and pale- to dark-brown (7.5-10YR) clay loam to silty clay loam and cobble to boulder gravel. Gravel clasts are dominated by limestone, white to yellow gypsum are interbedded throughout the unit. The dark gray shale typical of the lower section intertongues with the metamorphic rocks, and sandstone along the northern flank of the Sandia Mountains. Poorly exposed, inset against older eastern- underlying sandstone of the Dakota Formation (Kd) and the upper contact is gradational. Unit thickness is highly variable regionally Tz margin piedmont alluvium (Qpo1), and overlies a formerly broad, northwest-sloping pediment surface cut on Santa Fe Group and and across the study area, ranging from 850 ft (260 m) west of Placitas to 1,850 ft (565 m) in the Hagan embayment. Thickness near Base not exposed

older rocks. The western margin of unit is truncated by a buttress unconformity that probably formed during deposition of the Edith the Village of Placitas is intermediate. Miocene Formation (Qre). Deposit surface is slightly dissected, exhibits subdued bar-and-swale topography. Soils are moderately developed and exhibit weak Stage III carbonate morphology and many to continuous, thick clay films. Geomorphic surface Q5 of Connell Major unconformity Kd Dakota Formation — Medium-bedded, pervasively silica-cemented, medium-grained, yellowish-gray to orange-yellow quartz arenite. 23.7 (1995, 1996). Generally thickens to the northwest, from 7-20 ft (2-6 m). Thin interbeds of dark-gray lower Mancos Shale (Kml) are common. Sandstones are well cemented and weather to angular and blocky ridges. Unit thickness ranges from 75 ft (23 m) west of Placitas, to less than 25 ft (8 m) in the Hagan embayment. . Oligocene Te Tmi Older eastern-margin piedmont alluvium, middle subunit (middle to lower Pleistocene) — Poorly to moderately sorted and Qpo2 moderately consolidated deposits of brownish-yellow to yellowish-brown (10YR) gravel and sandy clay loam. Gravel clasts are 36.6 predominantly granite, metamorphic, and subordinate limestone. Locally contains grussified granite and split metamorphic clasts. Upper Jurassic Eocene Tg Very poorly exposed and mostly buried by eastern-margin piedmont alluvium (Qpy and Qpm) on the hangingwall of the Rincon 57.8 fault (NW1/4, Section 12, T12N, R5E). Soils are strongly developed and locally exhibit Stage III to IV carbonate morphology.

Geomorphic surface Q4 of Connell (1995, 1996). Estimated thickness is 7 ft to more than 45 ft (2-14 m). . Paleogene Paleocene Jm Morrison Formation, undivided — Three members are commonly recognized in northern New Mexico but are not differentiated in this map area. In descending stratigraphic order, the members are: the Jackpile Sandstone, the Brushy Basin Shale, and the Salt Wash 66.4 Older eastern-margin piedmont alluvium, older subunit (lower Pleistocene) — Moderately consolidated deposits of very Qpo Sandstone (the Westwater Canyon Sandstone of former usage, Lucas et al., 1995). The uppermost Jackpile Sandstone is a distinctive 1 pale-brown to brown (7.5-10YR) sandy clay loam to silty clay loam and poorly sorted, subangular to subrounded, limestone cobble gray-white, kaolinitic, fine- to medium-grained sandstone with a thickness of about 70 ft (21 m) near Placitas. The Brushy Basin member to boulder gravel. Gravel clasts are predominantly granite, metamorphic, and limestone. Unit is poorly exposed and forms a is a gray, green, and maroon mudstone and shale, with interbedded and intercalated gray to tan sandstone. Thickness is about 240 ft discontinuous gravelly veneer overlying a formerly extensive pediment surface near the Village of Placitas, as well as a strath just (73 m) near Placitas. The Salt Wash Sandstone is a gray to yellow-buff, medium-grained and weakly cemented sandstone, with a unit south of Las Huertas Creek. Inset against the gravel of Lomos Altos (Tsla) and inset by eastern-margin piedmont alluvium (Qpm). thickness of 215 ft (66 m) near Placitas. The Recapture Shale member has been redefined by Lucas et al. (1995) as the Summerville Kmf Soils are partially stripped and exhibit Stage II or III carbonate morphology. Commonly exposed on the footwalls of the Valley Formation of the upper San Raphael Group (Lucas and Anderson, 1997). However, due to poor exposure in the study area, it remains View, Rincon, and Lomos faults. Deposit surface is moderately dissected and is about 30-105 ft (9-32 m) above local base level. undifferentiated from the Morrison Formation. The Summerville Formation is approximately 325 ft (100 m) thick and consists of purple- Geomorphic surface Q3 of Connell (1995, 1996). Thickness is variable, up to 7 ft (2 m). MAP UNIT DESCRIPTIONS gray, red-brown, and green-gray mudstone interbedded with tan, gray, and greenish-gray, very fine grained sandstone. Total thickness Kpl of the Morrison and Summerville formations combined is relatively uniform regionally, ranging from about 850 ft (260 m) near Placitas Upper Santa Fe Group to 780 ft (240 m) in the Hagan embayment. Km CENOZOIC DEPOSITS Western basin-margin deposits (Arroyo Ojito Formation) u Middle Jurassic Neogene (Quaternary and Tertiary) System Arroyo Ojito Formation, undivided (lower Pleistocene to upper Miocene) — Cross section only. Base of unit is not exposed in QTo Khd Colluvial, landslide, eolian, and anthropogenic deposits map area. Estimated thickness is approximately 4,200 ft (1,280 m). Divided into two members in the map area. .

Jt Todilto Formation, undivided — Two members are commonly recognized in north-central New Mexico (Lucas et al., 1995), but are Cretaceous QToc Arroyo Ojito Formation, Ceja(?) Member (lower Pliocene to lower Pliocene) — Light-red to reddish-yellow (2.5-7.5YR), not differentiated in the map area. In descending stratigraphic order, the two members are the Tonque Arroyo Member and Luciano Km Thin surficial deposits derived from wind and mass-movement processes, or extensive areas disturbed by open-pit aggregate mining or moderately consolidated, slightly cemented, slightly tilted, stratified sandstone and pebbly sandstone with minor siltstone and Mesa Member. The Luciano Mesa Member is a medium-gray to olive-gray, laminated, fetid, micritic limestone. Dark-brown to black l construction. claystone interbeds. Gravel clasts are dominated by subangular to subrounded red granite, light-gray tuff, and basalt with carbonaceous mud is interbedded with limestone laminations near the base and gypsum interlayers are present from the middle to the subordinate chert, sandstone and minor quartzite. Conformably overlies the Loma Barbon Member of the Arroyo Ojito Formation top of the limestone member. The Tonque Arroyo Member is locally present as a white gypsum bed. Upper and lower contacts are (QTob) and is recognized by fairly abrupt increase in gravel content. Tentatively correlated to Kelley’s (1977) Ceja Member sharp. The unit is included in the middle San Raphael Group of Lucas and Anderson (1997). Thickness of the Luciano Mesa Member Kd af Artificial fill (Historic) — Dumped fill and areas affected by human disturbances. Locally mapped where areally extensive or geologic contacts are obscured. although stratigraphic position is ambiguous. Unit could also be a coarse-grained lens of gravely sandstone within the Loma Barbon ranges from 5 ft (1.5 m) southwest of the Village of Placitas, to about 20 ft (6 m) just east of the Cuchilla de San Francisco. Where Member (QTob). Approximately 40-60 ft (12-18 m) thick in map area. present, the Tonque Arroyo member is as much as 45 ft (14 m) thick. Total unit thickness is up to 65 ft (20 m). . daf Disturbed land and artificial fill, undivided (Historic) — Dumped fill and areas affected by open-pit aggregate mining or construction. Locally mapped where disturbance is areally extensive or geologic contacts are obscured. QTob Arroyo Ojito Formation, Loma Barbon Member (lower Pleistocene to upper Miocene) — Well consolidated, weakly to Entrada Formation — Variably colored, very fine- to fine-grained, weakly cemented, crossbedded, eolian, quartz sandstone with Jm moderately cemented, yellowish-brown to yellowish-red and reddish-brown (5-10YR), fine-grained silty sandstone with interbedded Je coarser-grained components. Near Placitas, the Entrada Formation is characterized by three distinct units differentiated by color: a lower Eolian sand (Holocene) — Unconsolidated, light-brown to light yellowish-brown (10YR), moderately to well sorted, fine-to medium- mudstone and scattered, lensoidal, weakly to well cemented, cobbly to bouldery sandstone interbeds. Gravel clasts are predominantly unit (75 ft or 23 m) of pale reddish-brown to grayish-pink sandstone, a middle unit (15 ft or 4.5 m) of gray-green sandstone, and an

Qe ° ° MESOZOIC grained sand primarily recognized as low-relief narrow dunes west of the Rio Grande. Soil development is very weak to nonexistent. subangular red granite, subrounded basalt and light-gray tuff, and minor sandstone derived from the northwestern margin of the upper unit (30 ft or 9 m thick) of grayish-yellow or light-tan sandstone. Due to the local dip of 20 to 30 , the Entrada Formation forms Jt Variable thickness, ranging from 0-16 ft (0-5 m). Albuquerque Basin and eastern slope of the Sierra Nacimiento. Named after a succession of reddish-brown sandstone, gravel, round, nonvegetated slopes rather than the cliffs and ledges typical of other localities. Included in the lower San Raphael Group of

and mudstone exposed just north of Loma Barbon. A primary airfall lapilli tuff (Locality B-1, SE1/4, SW1/4, NW1/4, Section Lucas and Anderson (1997). The contact with the underlying Chinle Group (ˇ cp) is disconformable. Total unit thickness ranges from Jurassic 40 39 ± Eolian sand and stream alluvium, undivided (Holocene to uppermost Pleistocene) — Unconsolidated to poorly consolidated, 10, T13N, R3E), present about 10 ft (3 m) below Ceja(?) Member deposits (QToc(?)), yields a Ar/ Ar date of 6.82 0.04 about 120 ft (37 m) near Placitas, to 71 ft (22 m) in the Hagan embayment. Qae Ma (NMGRL 8925, W.C. McIntosh, 1998, written communication) and is tentatively correlated with the Peralta Tuff Member of Je moderately to well sorted, light reddish-brown to light-brown (7.5-10YR), fine- to medium-grained sand and silty sand with scattered 40 39 ± pebbles that commonly forms a relatively thin, discontinuous mantle over upland areas west of the Rio Grande. Soil development is weak the Bearhead Rhyolite. A recycled subrounded rhyodacite(?) clast (Locality B-4) yields an Ar/ Ar date of 4.59 0.21 Ma (Bw and Bwk horizons) with maximum Stage I carbonate morphologic development. Surface is commonly stabilized by vegetation (NMGRL 9136, W.C. McIntosh, 1998, written communication). Interfingers with, and is overlain by axial-fluvial deposits (QTsa), Upper Triassic where not disturbed by human activity. May locally contain hydrocollapsible soils. Mapped only where areally extensive or thick. which are exposed east of the inner valley of the Rio Grande. Correlative deposits (unit QTst of Cather and Connell, 1998) are overlain by the basalt of Santa Ana Mesa (Tbsa). Locally includes thin, discontinuous lenses of unit QTsa along the margins of the ˇcp Variable thickness, ranging from 0-16 ft (0-5 m). ˇcp Chinle Group, undivided Petrified Forest Formation and Correo Sandstone — Predominantly reddish-brown mudstone interbedded inner valley of the Rio Grande. Estimated hydraulic conductivity is poor to moderate. Base is not exposed but is at least 425 m with thin subordinate sandstone and limestone-pebble conglomerate. The formation is only partially exposed near Placitas due to faulting. thick in borings (e.g., wells RRU12 and SAP2). Thickness and lithologic descriptions presented here are from the Hagan embayment. Although three informal subunits are recognized Landslide debris (upper to middle Pleistocene) — Poorly consolidated and very poorly sorted, sand, brecciated Santa Fe Group EFERENCES ˇz Qls deposits, and minor mud deposited by mass-movement processes, commonly along steep hillslopes. Locally forms rotated (Toreva blocks near Placitas that are distinct hydrostratigraphic units, they are not differentiated at the surface. The upper unit is a thick reddish-brown R Tobc Syntectonic colluvial wedge unit (upper Miocene to Pliocene) — Reddish-brown to orange-brown (5-10YR) sandstone and mudstone, overlain by relatively thin intervals of reddish-orange siltstone and a reddish-brown to tan coarse sandstone (Correo Sandstone

in Sections 8 and 9, T13N, R4E) blocks of gravity-transported basalt and Santa Fe Group sediments that exhibit hummocky topography Triassic mudstone associated with the hanging wall of the Luce fault (Section 11, T13N, R03E). Pinches out east of the Luce fault and is equivalent according to Picha, 1982). The middle unit consists of medium-grained moderately cemented sandstone interbedded with and bowl-shaped closed depressions along headwall scarps. Locally subdivided into older (Qls1) and younger (Qls2) units. Arrows Armstrong, A. K., and Mamet, B. L., 1974, Biostratigraphy of the Arroyo Peñasco Group, Lower Carboniferous (Mississippian), North-Central New Mexico: indicate direction of movement. Estimated thickness ranges from 20-100 ft (6-30 m). interpreted to be an intra-formational colluvial wedge associated with fault movement within the Loma Barbon Member (QTob). minor mudstone. The lower unit is a reddish-brown to purple to greenish-gray mudstone interbedded with silty to fine-grained sandstone. in: New Mexico Geological Society, 25th Field Conference Guidebook, p. 145-158. Thickness ranges from 0 to 46 ft (14 m). Gypsum and limestone-conglomerate lenses, characteristic of the Petrified Forest Formation, are pervasive throughout the unit. The lower ˇm contact with the underlying Agua Zarca Formation (ˇ z) is gradational and interfingering. The formation varies regionally in thickness Bachman, G. O., and Mehnert, H. H., 1978, New K-Ar dates and the late Pliocene to Holocene geomorphic history of the central Rio Grande region, New Qca Colluvium and alluvium, undivided (Holocene to upper-middle Pleistocene) — Poorly consolidated, poorly sorted and stratified, Mexico: Geological Society of America Bulletin, v.89, p. 283-292. fine- to coarse-grained, clast- and matrix-supported deposits derived from a variety of mass-movement hillslope processes, including Axial-fluvial deposits (ancestral Rio Grande) from about 1,300 ft to 1,650 ft (400 m to 500 m), and in the Hagan embayment is measured at 1,590 ft (485 m), Picha (1982). debris flow, shallow slump and creep. Deposits are delineated by sedimentary character and surface morphology. Gravel clasts are Cather, S. M., 1997, Toward a hydrogeologic classification of map units in the Santa Fe Group, Rio Grande rift, New Mexico: New Mexico Geology, v. typically angular and composition generally reflects local upslope provenance. Locally present on the eastern slope of Sandia Mountains Axial-fluvial deposits of the ancestral Rio Grande (lower Pleistocene to upper Miocene(?)) — Variable proportions of poorly Chinle Group, Agua Zarca Formation — Medium-grained, tan to white and light grayish-pink, thin- to medium-bedded quartz 19, n. 1, p. 15-21. QTsa ˇz arenite and feldspathic arenite with minor interbedded reddish-brown mudstone. Interbedded mudstone is similar to the Petrified Ps where deposits commonly surround small unmapped bedrock inliers. May locally contain hydrocollapsible soils. Differentiated where to moderately consolidated, generally weakly cemented, very pale-brown to yellowish-brown (10YR) subhorizontally bedded to slightly Cather S. M., and Connell, S. D., 1998, Geology of the San Felipe Pueblo 7.5-minute quadrangle, Sandoval County, New Mexico: New Mexico Bureau Forest Formation (ˇ cp). The sandstone is dominant and is very well cemented with silica, forms major ridges, and typically is highly Psg areally extensive, thick, or obscures geologic contacts. Variable thickness, ranging from 0-16 ft (0-5 m). . east-tilted sand, gravel and mud deposited by the ancestral Rio Grande. Sand is typically well sorted and crossbedded. Sand is locally of Mines and Mineral Resources, Open-File Report DM-19, scale: 1:24,000. well cemented along faults (see Locality P-6). Gravel clasts are predominantly rounded quartzite, with volcanics (intermediate, silicic, fractured. The lower contact with the underlying Moenkopi is disconformable. The total unit thickness near Placitas is 220 ft (67 m). Pg Qcb Basaltic colluvium (Holocene to middle Pleistocene) — Poorly consolidated and sorted sedimentary breccia composed of angular and basaltic), minor metamorphic rocks, granite, and chert. Mudstone ranges in color from light brown to grayish green. Clast imbrication Connell, S. D., 1995, Quaternary geology and geomorphology of the Sandia Mountains piedmont, Bernalillo and Sandoval Counties, central New Mexico: to subangular basalt boulders that mantle slopes below the mesa-capping basalt of Santa Ana Mesa (Tbsa) along the southeastern measurements indicate generally south to southwest paleoflow. The presence of recycled clasts of lower Bandelier Tuff (Locality P-3, P- [M.S. Thesis] Riverside, University of California, 390 p., 3 plates. margin of Santa Ana Mesa. Variable thickness, ranging from 0-16 ft (0-5 m). 4, and P-5) and an Irvingtonian “aged” Glyptotherium (Locality B-5; Lucas et al., 1993, p. 6) indicate an early Pleistocene age for the Connell, S. D., 1996, Quaternary geology and geomorphology of the Sandia Mountains piedmont, Bernalillo and Sandoval Counties, central New Mexico: upper part of this unit. Similar fluvial deposits interfinger with western basin-margin deposits beneath the basalt of Santa Ana Mesa Middle and Lower Triassic (Tbsa). Correlative deposits to the north are late Miocene to early Pleistocene in age (Smith and Kuhle, 1998b). May be correlative New Mexico Bureau of Mines and Mineral Resources, Open-File Report 425, 414 p., 3 plates (open-file release of Connell, 1995). . Permian Py Pyl Alluvium of the Rio Grande Moenkopi Formation — Laminated to thick-bedded, maroon-brown, micaceous, fine-grained sandstone and siltstone intercalated with with axial-stream deposits of the Sierra Ladrones Formation (Machette, 1978) described along the southern margin of the Albuquerque ˇm Connell, S. D., 1997, Geology of the Alameda 7.5-minute quadrangle, Bernalillo and Sandoval Counties, New Mexico: New Mexico Bureau of Mines and minor reddish-brown mudstone. Sandstones and mudstones are moderately to weakly cemented and locally friable with generally low Pay Basin. Estimated hydraulic conductivity is moderate to high. Base is not exposed. Estimated thickness is 2,200 ft (670 m). Mineral Resources, Open-File Digital Map 10, scale 1:24,000. Fluvial deposits derived from the ancestral and modern Rio Grande. Unconformably overlies upper Santa Fe Group deposits (commonly porosity. Both upper and lower contacts are unconformable and regional thickness varies significantly. The unit is poorly exposed in Pa Loma Barbon Member and axial-fluvial deposits of the ancestral Rio Grande). Interfingers with eastern-margin piedmont alluvium and Transitional fluvial-piedmont deposits — Interfingered axial-fluvial deposits (QTsa) and Santa Fe Group eastern basin-margin piedmont the Placitas area and thickness ranges from at least 45 ft (14 m) near the Village of Placitas to 100 ft (30 m) in the Hagan embayment. Connell, S. D., Allen, B. D., Hawley, J. W., and Shroba, R. S., 1998, Geology of the Albuquerque West 7.5-minute quadrangle, Bernalillo County, New western-margin alluvium. Subdivided into six formations on the basis of inset relationships and, to a lesser extent, soil morphology. QTst Mexico: New Mexico Bureau of Mines and Mineral Resources, Open-File Report DM-17, scale: 1:24,000. deposits (QTspcs and QTsp). Transitional deposits are defined as the zone of overlap between the easternmost outcrops of axial river Las Padillas Formation (Historic to uppermost Pleistocene) — Unconsolidated to poorly consolidated, pale-brown (10YR), fine- to deposits and the westernmost outcrops of piedmont sandstone and conglomerate. Mudstone is commonly ambiguous as to its position Geissman, J. W., Brown, L., Turrin, B. D., McFadden, L. D., and Harlan, S., 1990, Brunhes chron excursion/polarity episode reco rded during the late ˛m

Qrp PALEOZOIC coarse-grained sand and rounded gravel with subordinate lensoidal interbeds of fine-grained sand, silt, and clay derived from the Rio within the facies tract (piedmont vs. axial), and is not a factor in delineating the transitional facies (Cather, 1997). A rounded pumice Pleistocene Albuquerque volcanoes, New Mexico, USA: Geophysical Journal Int.: v. 102, p. 73-88. clast from a lens of fluvial sand and gravel (Locality B-6) has been identified by 40Ar/39 Ar dating as the ca. 1.6 Ma lower Bandelier PALEOZOIC ERATHEM Qrp2 Grande. Recognized in drillholes and named for deposits underlying the broad inner valley floodplain near the community of Las Padillas Hibben, F. C., 1941, Evidences of early occupation in Sandia Cave, New Mexico, and other sites in the Sandia-Manzano region: Smithsonian Institute Tuff (W. C. McIntosh, 1995 written communication). Penn. ˛s in southwest Albuquerque (Connell et al., 1998). Unconformably overlies upper Santa Fe Group deposits (QTob and QTsa) and is Upper Permian Miscellaneous Collections, v. 99, n. 23, publication 3636, 44 p. Qrp1 commonly gravelly at the base. Underlying Santa Fe Group deposits may be locally cemented with calcium carbonate. Probably interfingers with stream alluvium of units QHa and Qay. Deposit surface (top) comprises the modern surface of aggradation for Rio Kelley, V. C., 1977, Geology of the Albuquerque basin, New Mexico: New Mexico Bureau of Mines and Mineral Resources, Memoir 33, 60 p. Eastern basin-margin piedmont deposits Ps San Andres Formation — Light gray to tan, thin- to medium-bedded limestone with interbedded grayish-white sandstone, similar to Grande fluvial deposits. Locally divided into older (Qrp1) and younger (Qrp2) subunits on the basis of inset relationships as estimated the Glorieta Formation (Pg), at the base. The limestones are well indurated, have a high fracture porosity, and are locally cavernous. Kelley, V. C., and Kudo, A. M., 1978, Volcanoes and related basalts of Albuquerque Basin, New Mexico: New Mexico Bureau of Mines and Mineral from available aerial photography. Also subdivided into modern channel deposits of the Rio Grande (Qrpr) and Rio Jemez (Qrpj). The lower contact with the Glorieta Formation is gradational. Unit thickness ranges from about 80 ft (24 m) near Placitas to 130 ft (40 Resources, Circular 156, 30 p, 2 plates. Ma Approximately 50-80 ft (15-24 m) thick. QTt Travertine and spring deposits (middle Pleistocene to Pliocene) — Light-gray nodular to massive limestone interlayered with mudstone. Prominent outcrop at the northern tip of the Cuchilla de San Francisco (Sections 14 and 15, T13N, R5E) where deposits m) in the Hagan embayment. Kelley, V. C., and Northrop, S. A., 1975, Geology of the Sandia Mountains and vicinity: New Mexico Bureau of Mines and Mineral Resources, Memoir Miss. Modern channel facies (Historic) — Unconsolidated sand and gravel within the active channel of the Rio Grande. . overlie and interfinger with Santa Fe Group eastern basin-margin piedmont deposits (QTspcs) on the hangingwall of the San Francisco 29, 136 p. Qrpr fault. Spring deposits are locally present along depositional contacts and faults. Variable thickness, up to 50 ft (15 m) thick. Glorieta Formation — White to grayish white, massively bedded, well-indurated, medium-grained, quartz arenite. In some localities, Pg Kelley, S. A., Chapin, C. E., and Corrigan, J., 1992, Late Mesozoic to Cenozoic cooling histories of the flanks of the northern and central Rio Grande rift, Qrp a greenish-yellow silty mudstone, 2 to 3 ft (60 to 90 cm) thick, occurs near the top of the formation. The sandstone is extremely well METASEDIMENTARY METAVOLCANIC PLUTONIC j Sandy floodplain alluvium of the Rio Jemez (Historic) — Unconsolidated sand and gravel at the mouth of the Rio Jemez. . cemented with silica, is often strongly fractured, and forms prominent ridges and ledges. The lower contact with the Yeso Formation (Py) Colorado and New Mexico: New Mexico Bureau of Mines and Mineral Resources, Bulletin 145, 39 p. Qss Suela Alluvium (lower Pleistocene) — Moderately consolidated and weakly cemented deposits of brown, very pale-brown to white (7.5YR-2.5Y) sandy loam, sand and subrounded to subangular cobble to pebble gravel overlying remnants of extensive, relatively is disconformable and sharp. Unit thickness varies from about 50 ft (15 m) near Placitas to 35 ft (11 m) in the Hagan embayment. Kirby, E., Karlstrom, K. E., and Andronicus, C. L., 1995, Tectonic setting of the Sandia pluton: An orogenic 1.4 Ga granite in New Mexico: Tectonics, v. 14, Qra Arenal Formation (upper Pleistocene) — Poorly consolidated deposits of very pale-brown to yellow (10YR) sandy pebble to cobble gravel recognized along the northwestern margin of the Rio Grande inner valley. Named for exposures just west of the Arenal Main smooth, northwest-sloping pediment surface that cuts across the trace of the Placitas fault. Gravel clasts contain abundant subrounded p. 185-201. Canal in southwest Albuquerque (Connell et al., 1998), where it underlies Lambert’s (1968) Primero Alto terrace surface. Gravel clasts to subangular limestone, granite, sandstone, and metamorphic rocks. Limestone clasts are typically pitted, and granite clasts are locally grussified. The basal contact is unconformable along the northern flank of the Sandia Mountains, but becomes conformable with the Lower Permian Kudo, A. M., Kelley, V. C., Damon, P. E., and Shafiquillah, M., 1977, K-Ar ages of basalt flows at Canjilon Hill, Isleta volcano, and Cat Hills volcanic field, are primarily rounded quartzite and subrounded volcanic rocks (commonly welded tuff and rare pumice) with minor granite. Soil Albuquerque-Belen Basin, central New Mexico: Isochron/West, n. 18, p. 15-16. development is very weak with Stage I carbonate morphology. The basal contact is approximately 50 ft (15 m) above the top of the underlying axial-fluvial deposits (QTsa) northwest of the Escala and Lomos faults. The deposit surface (top) forms a broad, northwest- Las Padillas Formation (Qrp, Rio Grande floodplain). Approximately 10-20 ft (3-6 m) thick. sloping constructional surface herein named the Las Huertas geomorphic surface. The Las Huertas geomorphic surface is commonly Lambert, P. W., 1968, Quaternary stratigraphy of the Albuquerque area, New Mexico [Ph.D. dissertation]: Albuquerque, University of New Mexico, 329 buried by thin veneer of light-brown eolian sand, diverges downstream of Las Huertas Creek, between about 110-165 ft (34-50 m), Yeso Formation, undivided — Two members of the Yeso Formation are recognized but not divided in the map area: the San Ysidro Ys Yp Py Member, and the underlying Meseta Blanca Member. The San Ysidro Member is a friable, orange-brown, laminated to thickly bedded, p. Los Duranes Formation (upper(?) to upper-middle Pleistocene) — Poorly to moderately consolidated deposits of light reddish- and is underlain by moderately to strongly developed soils exhibiting III+ carbonate morphology. In the map area, the Las Huertas Qrd geomorphic surface is interpreted to mark the end of upper Santa Fe Group deposition and the initiation of Quaternary incision by the silty to fine-grained sandstone and interbedded siltstone with minor clay-rich and limestone layers. A moderately cemented coarse Lucas, S. G. and Anderson, O. J., 1997, The Jurassic San Rafael Group, Four Corners region: in: New Mexico Geological Society, 48th Field Conference brown, pale-brown to yellowish-brown (5-10YR) gravel, sand, and minor sandy clay derived from the ancestral Rio Grande. Locally sandstone occurs at the base. The Meseta Blanca Member is lithologically distinct and consists of a light-orange to gray-white, medium- covered by discontinuous veneer of undivided alluvium and eolian deposits (Qae). Interfingers with, and is overlain by, western-margin Rio Grande. Bar-and-swale topography is absent and soils exhibit Stage III+ carbonate morphology, and very few thin silica and clay Guidebook, p. 115-132. films. Overlies Bandelier Tuff-bearing piedmont and fluvial deposits (QTsp and QTsa) and is thus, younger than about 1.1 Ma. to coarse-grained, moderately cemented sandstone. Picha (1982) mapped an informal lower Yeso member as a separate unit in the alluvium (Qam). Unconformably overlies deposits of the Loma Barbon Member (QTob). Map relationships and scattered drill-hole data cs Lucas, S. G., Anderson, O. J., and Pigman, C., 1995, Jurassic Stratigraphy in the Hagan Basin, North-Central New Mexico: in: New Mexico Geological Mesoproterozoic Geomorphic surface Q2 of Connell (1995, 1996). Generally thickens to the northwest, from about 7 to 16 ft (2-5 m). . Hagan embayment (Pyl) that is similar to the San Ysidro Member. The lower contact with Abo Formation (Pa) is conformable, but is suggests that the basal contact forms low-relief strath approximately 20 ft (6 m) above the top of the Las Padlillas Formation (Qrp, Rio commonly difficult to discern because of similar lithologies. Total thickness is 680 ft (207 m) in the Hagan embayment. Society, 46th Field Conference Guidebook, p. 247-255. Grande floodplain). This basal contact is inset approximately 100 ft (30 m) below the base of the Edith Formation (Qre). Provisionally Gravel of Lomos Altos (upper Pliocene) — Well consolidated deposits of very pale-brown to brown (10YR-2.5Y), sandy clay loam, Lucas, S. G., Williamson, T. E., and Sobus, J., 1988, Late Pleistocene (Rancholabrean) mammals from the Edith formation, New Mexico: New Mexico Journal correlated with the Los Duranes Formation of Lambert (1968). Deposit contains the Rancholabrean mammal Bison latifrons (Locality B- Tsla Yeso Formation, lower member — Informal lower sandstone member of the Yeso Formation is lithologically similar to the San 7; Smartt et al., 1991, SW1/4, NE1/4, Section 19, T13N, R4E), which supports a middle Pleistocene deposit age. Correlative deposits sandy loam and subrounded to subangular, limestone-dominated, cobble to pebble gravel overlying remnants of a formerly broad Pyl of Science, v. 28, n. 1, p. 51-58. pediment cut on Santa Fe Group eastern basin-margin piedmont deposits (Tspu , Tsp ) on Lomos Altos. The basal contact is about 260- Ysidro Member (as described above). Differentiated east of the Cuchilla de San Francisco (see Picha, 1982). . to the south locally bury the late-middle Pleistocene (156±20 ka, Peate et al., 1996) basalt of the Albuquerque volcanoes (Connell, c c Lucas, S. G., Williamson, T. E., and Sobus, J., 1993, Plio-Pleistocene stratigraphy, paleoecology, and mammalian biochronology, Tijeras Arroyo, Albuquerque 328 ft (80-100 m) above local base level, is inset against Santa Fe Group piedmont deposits (Tspu ), and is recognized on the footwalls PROTEROZOIC 1996, unpubl. data). Approximately 20-23 ft (6-7 m) thick in map area. c area, New Mexico: New Mexico Geology, v. 15, n. 1, p. 1-8. Xms Xas Xss Xr Xa of the Lomos, Escala, and southern Valley View faults. Soils are strongly developed, partially stripped and exhibit Stage IV+ carbonate Pa Abo Formation — Predominantly a reddish-brown mudstone alternating with grayish-white to light-orange lenticular beds of medium- morphology. Unit may be equivalent to the Tuerto gravel of Stearns (1953) or the gravel of Lookout Park of Smith and Kuhle (1998a). to coarse-grained sandstone. The Abo Formation is distinguished from the Yeso Formation (Py) based primarily on a slight color change Machette, M. N., 1978, Geologic map of the San Acacia Quadrangle, Socorro County, New Mexico: U.S. Geological Survey Geologic Quadrangle Map Menaul Formation (upper to upper-middle Pleistocene) — Poorly consolidated deposits of yellowish-brown (10YR) pebble gravel from orange-brown to reddish-brown and a higher proportion of coarser-grained orange or white sandstone. The sandstone is locally Qrm and pebbly sand derived from the ancestral Rio Grande. Named by Lambert (1968) for exposures to the south in Albuquerque. Gravel Correlative deposits west of the Escala fault are probably buried beneath the Suela alluvium (Qss) and piedmont deposits of unit QTspcs. GQ-1415, scale 1:24,000. Geomorphic surface QT1 of Connell (1995, 1996). Thickens northward from 13-60 ft (4-18 m) thick. . conglomeratic and arkosic in the lower part. The lower contact with the Madera Formation (˛ m ) is gradational and interfingering, with clasts are dominated by rounded quartzite pebbles that are generally smaller in size than pebbles and cobbles in the Edith Formation about 20% limestone units interbedded in reddish-brown mudstone over the lower 80 ft (25 m). The top of the lowermost laterally Menne, B., 1989, Structure of the Placitas area, northern Sandia uplift, Sandoval County, New Mexico [M.S. thesis]: Albuquerque, University of New Mexico,

(Qre). Forms discontinuous, probably lensoidal, exposures along the eastern escarpment of the inner valley escarpment of the Rio Paleoproterozoic Piedmont deposits, undivided (lower Pleistocene to Miocene) — Subhorizontally stratified to slightly east-tilted, reddish-brown to continuous and relatively thick limestone bed is chosen as the Madera Formation contact. Unit thickness on Cuchilla de San Francisco 163 p. Grande. The basal contact is approximately 85-118 ft (26-36 m) above the top of the Las Padillas Formation (Qrp, Rio Grande QTsp yellowish-brown and very pale-brown (7.5-10YR) conglomerate, gravelly sandstone, and sandstone with subordinate siltstone and rare is 1,070 ft (325 m), Picha (1982). 238 230 floodplain). Poorly exposed remnants of a partially eroded soil on eastern-margin piedmont alluvium (Qpm1) indicates that the Menaul Peate, D. W., Chen, J. H., Wasserburg, G. J., and Papanastassiou, D. A., 1996, U- Th dating of a geomagnetic excursion in Quaternary basalts of Formation unconformably overlies Qpm . Conformably overlain by eastern-margin piedmont alluvium (Qpm ), and is inset by younger mudstone. Conglomerate clasts are predominantly composed of subangular limestone, metamorphic rocks, with minor granite and the Albuquerque Volcanoes field, New Mexico (USA): Geophysical Research Letters, v. 23, n. 17, p. 2271-2274. . 1 2 sandstone. Clast imbrications indicate generally west to southwest paleoflow. Includes unit Tsp on cross section. May be correlative with Upper and Middle Pennsylvanian stream alluvium (Qay). May represent lenses of fluvial gravel associated with the Los Duranes Formation (Qrd) east of the Rio Grande. Picha, M. G., 1982, Structure and stratigraphy of the Montezuma salient-Hagan basin area, Sandoval County, New Mexico [M.S. thesis]: Albuquerque, Thickness is generally less than 10 ft (3 m). piedmont-slope and alluvial fan deposits of the Sierra Ladrones Formation (Machette, 1978) exposed at the southern margin of the Albuquerque Basin. Thickens to the east and interfingers with axial-fluvial deposits (QTsa) to the west. Moderate to low estimated University of New Mexico. Madera Formation, undivided — An informal upper arkosic limestone member and a lower gray limestone member of the Madera Edith Formation (middle Pleistocene) — Poorly to moderately consolidated, locally cemented deposits of pale-brown to yellowish- hydraulic conductivity. Thickness is variable and estimated to range from 3,000-7,000 ft (915-2,135 m) thick. Divided into four subunits ˛m Read, A. S., Karlstrom, K. E., Ilg, B., 1999 (in press), Mississippian Del Padre Sandstone or Proterozoic Quartzite?: minipaper in: New Mexico Geological Qre based on dominant deposit texture (see Cather, 1997). Formation are recognized, but not differentiated in this study area. The upper arkosic limestone member is gray, greenish-gray, olive- brown (10YR) gravel, sand and sandy clay derived from the ancestral Rio Grande. Forms laterally extensive outcrops along the inner gray, tan, and buff-brown fossiliferous limestone (57% of upper member) interbedded with intervals of subarkosic sandstone and Society, 50th Field Conference Guidebook. valley escarpment of the Rio Grande that are physically correlated to Lambert’s (1968) type locality to the south (see Connell, 1997; Piedmont deposits, conglomerate subunit — Predominantly conglomerate (conglomerate:sandstone ratio is greater than 2) with mudstone. Limestone is thinly to thickly bedded and massive with sparsely disseminated chert. Sandstones and mudstones vary from Smartt, R. A., Lucas, S. G., Hafner, D. J., 1991, The giant Bison (Bison latifrons) from the middle Rio Grande Valley of New Mexico: The Southwestern Connell et al., 1998). Forms an upward-fining succession consisting of a 7-26 ft (2-8 m) thick, basal quartzite-rich, cobble gravel that QTspc reddish-brown to maroon to greenish-gray and gray and are lenticular and laterally discontinuous. Arkosic sandstones are typically Naturalist, v. 36., n. 1, p. 136-137. grades up-section into a 13-32 ft (4-10 m) thick succession of yellowish-brown (10YR) sand and reddish-brown mud. The upper contact subordinate sandstone and very rare mudstone interbeds. Conglomerate clasts contain pebbles, cobbles, and boulders of lithologies similar to clasts in underlying Santa Fe Group eastern basin-margin piedmont deposits (QTspcs). Sandstone is coarse to very coarse coarse- to medium-grained and commonly contain granules and pebbles. The lower gray limestone member is a gray, ledge-forming, is locally marked by a thin, white (5Y) diatomite. Gravel clasts contain abundant rounded quartzite (about 30%) and volcanic rocks cherty limestone separated by thinner less resistant intervals of light-brown, pale greenish-brown, tan, greenish-gray, and gray argillaceous Smith, G. A., and Kuhle, A .J., 1998a, Geology of the Santo Domingo Pueblo SW 7.5-minute quadrangle, Sandoval County, New Mexico: New Mexico (about 40%) with subordinate granite, metamorphic, and sandstone clasts, and very rare rounded welded Bandelier Tuff. Unit and typically crossbedded or horizontally laminated. Matrix-supported conglomerate is common and interpreted to represent debris flow deposits. limestone. A distinct 7 ft (2 m) thick interval of medium- to coarse-grained, green, subarkosic sandstone lies 160 ft (50 m) below the Bureau of Mines and Mineral Resources, Open-file Digital Geologic Map OF-DM 26, scale 1:24,000. unconformably overlies upper Santa Fe Group deposits (QTob and QTsa), and is conformably overlain by eastern-margin piedmont top of the lower gray limestone member and provides a marker for the lower unit. The top of the lower gray limestone member is placed Smith, G. A., and Kuhle, A. J., 1998b, Hydrostratigraphic implications of new geologic mapping in the Santo Domingo Basin, New Mexico: New Mexico alluvium (Qpm ). A partially exposed buttress unconformity between eastern-margin piedmont alluvium (Qpm ) and upper Santa Fe 1 2 Piedmont deposits, conglomerate and sandstone subunit — Sub-equal conglomerate and sandstone. Conglomerate is typically at the top of the uppermost cliff-forming limestone exposed on the western rim of the Crest of Montezuma (referred to locally as Geology, v. 20, n. 1, p. 21-27. Group deposits (QTob, QTsa, and QTsp) locally marks the eastern extent. Basal contact is generally well exposed and forms a low- QTspcs Montezuma Mountain) and is also approximately coincident with the top of Cuchilla Lupe. The upper arkosic limestone member is relief strath approximately 40-80 ft (12-24 m) above the top of the Las Padillas Formation (Qrp, Rio Grande floodplain). Locally contains poorly sorted and clast supported, consisting primarily of pebbles and cobbles of Paleozoic limestone, sandstone, siltstone, and chert, and Proterozoic granite, gneiss, phyllite, and schist. Proterozoic detritus becomes more abundant in the southern part of approximately 615 ft (187 m) thick and the lower gray limestone member is approximately 645 ft (197 m) thick. Total unit thickness is Spiegel, Z., 1961, Geology of the lower Jemez River area, New Mexico: New Mexico Geological Society, Guidebook 12, p. 132-138. . Rancholabrean fossils (Lambert, 1968; Lucas et al., 1988). Moderately developed soils on overlying eastern-margin piedmont deposits 1,260 ft (385 m) on the Crest of Montezuma (Picha, 1982). Steiger, R .H., and Wasserburg, G. J., 1966, Systematics in the Pb208-Th207-U235, and Pb206-U238 systems: Journal of Geophysical Research, v. 71, p 6065- (Qpm ) suggest a middle Pleistocene age for unit. Variable thickness, up to 10-40 ft (3 to 12 m). the quadrangle. Sandstone is horizontally laminated or trough crossbedded, moderately to poorly sorted, and commonly pebbly. 1 Mudstone is rare. Volcanic ash (Locality P-2) is present near the top and may be correlative to the Bandelier Tuff (Dunbar, 1997, 6090. Sandia Formation — Consists of a variety of lithologies including, in descending stratigraphic order: interbedded brown claystone and Lomatas Negras Formation (middle Pleistocene) — Moderately consolidated and weakly cemented sandy pebble to cobble gravel personal communication). On the basis of stratigraphic position (e.g., stratigraphically above recycled lower Bandelier Tuff clasts ˛s Qrl in unit QTsa), this ash is probably correlative to the ca. 1.1 Ma upper Bandelier Tuff. gray limestone, massive gray limestone, and a lower olive-brown to gray, subarkosic, fine- to coarse-grained sandstone. The contact Stearns, C. E., 1953, Tertiary geology of the Galisteo-Tonque area: New Mexico: Geological Society of America Bulletin, v. 64, p. 459-508. . primarily composed of subrounded to rounded quartzite, volcanic rocks, granite and minor basalt. Discontinuously exposed and with overlying Madera Formation (˛ m ) is chosen at the base of the lowest thick limestone ledge. The lower contact is unconformable Tilton, G. R., and Grunenfelder, M .H., 1968, Uranium-lead ages, Science, v. 159, p. 1458-1461. recognized as a lag of rounded quartzite-bearing gravel approximately 230-245 ft (70-75 m) above the top of the Las Padillas Formation Piedmont deposits, sandstone subunit — Sandstone (conglomerate:sandstone ratio is less than 0.5), with subordinate siltstone. with the Arroyo Peñasco Group, where present, or Proterozoic basement. Sandia Formation limestones are distinct from the Madera (Qrp, Rio Grande floodplain). Basal contact forms a low-relief strath cut onto the Loma Barbon Member (QTob). Unconformably(?) QTsps Formation limestones as they are typically thinner-bedded, clast-supported, greenish, and contain abundant siliciclastic material. Unit is U.S. Geological Survey and Sial Geosciences, Inc., 1998, Description of digital aeromagnetic data collected north and west of Albuquerque, New Mexico: overlain by western-margin alluvium (Qam). Correlative deposits to the south underlie the late-middle Pleistocene (156±20 ka, Peate Sandstone is mostly horizontally laminated with subordinate trough and planar crossbedding. Conglomerate occurs in shallow, lenticular beds, is mostly clast supported, and consists dominantly of pebbles of Paleozoic sedimentary rocks and Proterozoic 193 ft (59 m) thick on the Crest of Montezuma. U.S. Geological Survey, Open-File Report 97-286, http://www.ngdc.noaa.gov/seg/potfld/ad_sys.html. . et al., 1996) Albuquerque volcanoes basalt. Unit may be correlative to fluvial terrace deposits Qta1 of Smith and Kuhle (1998a), which contains the ca. 602 ka Lava Creek B ash. Generally less than 16 ft (5 m) thick. crystalline rocks. Siltstone is massive to faintly laminated and forms tabular to broadly lenticular beds. .

QTspsm Piedmont deposits, siltstone and mudstone subunit — Siltstone and mudstone with rare sandstone. .